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. 2023 Jan 19;1(1):60–73. doi: 10.1038/s44221-022-00001-4

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© The Author(s) 2023

Open Access This article is licensed under a Creative Commons Attribution 4.0 International License, which permits use, sharing, adaptation, distribution and reproduction in any medium or format, as long as you give appropriate credit to the original author(s) and the source, provide a link to the Creative Commons license, and indicate if changes were made. The images or other third party material in this article are included in the article’s Creative Commons license, unless indicated otherwise in a credit line to the material. If material is not included in the article’s Creative Commons license and your intended use is not permitted by statutory regulation or exceeds the permitted use, you will need to obtain permission directly from the copyright holder. To view a copy of this license, visit http://creativecommons.org/licenses/by/4.0/.

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Fig. 2 — a, Stable water isotope composition of investigated sites alongside all available measurements of springs, groundwater wells, mineral water and brewery wells and thermal deep wells; stable water isotope-derived recharge elevations after Yasuhara et al.³⁶ are indicated. Local meteoric water line (LMWL)³⁶: δ²H = 8 × δ¹⁸O + 15.1‰. Global meteoric water line (GMWL)⁵¹: δ²H = 7.93 × δ¹⁸O + 8.99‰. VSMOW, Vienna standard mean ocean water. b, Piper plot of the major ion composition of all available data on springs, groundwater wells, mineral water and brewery wells, and thermal deep wells. The fields of hydrochemical water types are separated by dashed lines and marked by numbered circles (see legend). Data points in a and b represent site-averaged values. All individual data points and corresponding references are provided in tabular form in Supplementary Data 1.