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                    <gco:CharacterString>Wainer, K.; D. Genty; D. Blamart; M. Daëron; M. Bar-Matthews; H. Vonhof; Y. Dublyansky; E. Pons-Branchu; L. Thomas; P. van Calsteren; Yves Quinif; N. Caillon</gco:CharacterString>
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        <gco:CharacterString>STUDY NOTES: Data contributed as part of SISAL v3 Global Speleothem Isotope and Trace Element Database (https://doi.org/10.25921/jajq-qg60). Notes from the SISAL database: Vil-stm11 (SISAL entity_id = 29): Detrital Th correction made only on the top two samples (dating_id = 8198 and 8199). U-Th ages for entity_id=29 were calculated using the following decay constants: 234U: 2.835*10^(-6)/yr, 238U: 1.55125*10^(-10)/yr, 230Th: 9.1952*10^(-6)/yr, 232Th: 4.9475*10^(-11)/yr. Decay constants are probably derived from the following papers: 230Th: Meadows et al.,1980, 234U: average value from De Bievre et al. 1971 and Lounsbury and Durham 1971. \\ Vil-stm1 (entity_id = 29): The normalisation to Ca for trace elements is assumed based on the best of our knowledge, contact with authors was not possible.\\ Vegetation: mainly oak and hornbeam forest, the part of the cave where stalagmite stm-1 was sampled is covered by grassland. Host rock cover thickness over the cave is given as an average in the sheet. The thickness reported in the paper is 25-45 m. 
ABSTRACT SUPPLIED BY ORIGINATOR: The Vil-car-1 flowstone core from Villars cave (SW France) provides one of the first European speleothem records extending back to 180 ka, based on U–Th TIMS and MC-ICP-MS measurements. The core offers a continuous record of Termination II and the Last Interglacial. The penultimate deglaciation is characterized by a prominent 5‰ depletion in calcite δ18O. Determining which specific environmental factors controlled such a large oxygen isotopic shift offers the opportunity to assess the impact of various factors influencing δ18O variations in speleothem calcite. Oxygen isotope analyses of fluid inclusions indicate that drip water δ18O remained within a very narrow range of ±1‰ from Late MIS6 to the MIS5 δ18O optimum. The possibility of such a stable behaviour is supported by simple calculations of various effects influencing seepage water δ18O. Although this could suggest that the isotopic shift in calcite is mainly driven by temperature increase, attempts to quantify the temperature shift from Late MIS6 to the MIS5 δ18O optimum by assuming an equilibrium relationship between calcite and fluid inclusion δ18O yield unreasonably high estimates of ∼20 °C warming and Late MIS6 cave temperatures below 0 °C; this suggests that the flowstone calcite precipitated out of thermodynamic equilibrium at this site. Using a method proposed by Guo et al. (submitted for publication) combining clumped isotope measurements, fluid inclusion and modern calcite δ18O analyses, it is possible to quantitatively correct for isotopic disequilibrium and estimate absolute paleotemperatures. Although the precision of these absolute temperature reconstructions is limited by analytical uncertainties, the temperature rise between Late MIS6 and the MIS5 optimum can be robustly constrained between 13.2 ± 2.6 and 14.6 ± 2.6 °C (1σ), consistent with existing estimates from Western Europe pollen and sea-surface temperature records.</gco:CharacterString>
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