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Climate of the Past the Magnesium Isotope Record of Cave VU Research Portal The magnesium isotope record of cave carbonate archives Riechelmann, S.; Buhl, D.; Schröder-Ritzrau, A.; Riechelmann, D.F.C.; Richter, D.K.; Vonhof, H.B.; Wassenburg, J.A.; Geske, A.; Spötl, C.; Immenhauser, A.M. published in Climate of the Past 2012 DOI (link to publisher) 10.5194/cp-8-1849-2012 document version Publisher's PDF, also known as Version of record Link to publication in VU Research Portal citation for published version (APA) Riechelmann, S., Buhl, D., Schröder-Ritzrau, A., Riechelmann, D. F. C., Richter, D. K., Vonhof, H. B., Wassenburg, J. A., Geske, A., Spötl, C., & Immenhauser, A. M. (2012). The magnesium isotope record of cave carbonate archives. Climate of the Past, 8, 1849-1867. https://doi.org/10.5194/cp-8-1849-2012 General rights Copyright and moral rights for the publications made accessible in the public portal are retained by the authors and/or other copyright owners and it is a condition of accessing publications that users recognise and abide by the legal requirements associated with these rights. • Users may download and print one copy of any publication from the public portal for the purpose of private study or research. • You may not further distribute the material or use it for any profit-making activity or commercial gain • You may freely distribute the URL identifying the publication in the public portal ? Take down policy If you believe that this document breaches copyright please contact us providing details, and we will remove access to the work immediately and investigate your claim. E-mail address: [email protected] Download date: 29. Sep. 2021 Clim. Past, 8, 1849–1867, 2012 www.clim-past.net/8/1849/2012/ Climate doi:10.5194/cp-8-1849-2012 of the Past © Author(s) 2012. CC Attribution 3.0 License. The magnesium isotope record of cave carbonate archives S. Riechelmann1, D. Buhl1, A. Schroder-Ritzrau¨ 2, D. F. C. Riechelmann3, D. K. Richter1, H. B. Vonhof4, J. A. Wassenburg1, A. Geske1, C. Spotl¨ 5, and A. Immenhauser1 1Ruhr-University Bochum, Institute for Geology, Mineralogy and Geophysics, Universitatsstraße¨ 150, 44801 Bochum, Germany 2Heidelberg Academy of Sciences, Im Neuenheimer Feld 229, 69120 Heidelberg, Germany 3Johannes Gutenberg University Mainz, Institute of Geography, Johann-Joachim-Becher-Weg 21, 55099 Mainz, Germany 4Faculty of Earth and Life Sciences, Vrije Universiteit Amsterdam, De Boelelaan 1085, 1081 HV, Amsterdam, The Netherlands 5Leopold-Franzens-University Innsbruck, Institute for Geology and Palaeontology, Innrain 52, 6020 Innsbruck, Austria Correspondence to: S. Riechelmann ([email protected]) Received: 30 April 2012 – Published in Clim. Past Discuss.: 22 May 2012 Revised: 12 October 2012 – Accepted: 27 October 2012 – Published: 20 November 2012 Abstract. Here we explore the potential of magnesium air temperature was the principal driver rather than rain- (δ26Mg) isotope time-series data as continental climate prox- fall amount. The alpine Pleistocene flowstones from Austria ies in speleothem calcite archives. For this purpose, a total of (SPA 52: −3.00 ± 0.73 ‰; SPA 59: −3.70 ± 0.43 ‰) are af- six Pleistocene and Holocene stalagmites from caves in Ger- fected by glacial versus interglacial climate change with out- many, Morocco and Peru and two flowstones from a cave in side air temperature affecting soil zone activity and weath- Austria were investigated. These caves represent the semi- ering balance. Several δ26Mg values of the Austrian and arid to arid (Morocco), the warm-temperate (Germany), the two δ26Mg values of the German speleothems are shifted to equatorial-humid (Peru) and the cold-humid (Austria) cli- higher values due to sampling in detrital layers (Mg-bearing mate zones. Changes in the calcite magnesium isotope signa- clay minerals) of the speleothems. The data and their inter- ture with time are compared against carbon and oxygen iso- pretation shown here highlight the potential but also the lim- tope records from these speleothems. Similar to other prox- itations of the magnesium isotope proxy applied in continen- ies, the non-trivial interaction of a number of environmental, tal climate research. An obvious potential lies in its sensitiv- equilibrium and disequilibrium processes governs the δ26Mg ity for even subtle changes in soil-zone parameters, a hitherto fractionation in continental settings. These include the dif- rather poorly understood but extremely important component ferent sources of magnesium isotopes such as rainwater or in cave archive research. Limitations are most obvious in the snow as well as soil and host rock, soil zone biogenic activ- low resolution and high sample amount needed for analysis. ity, shifts in silicate versus carbonate weathering ratios and Future research should focus on experimental and conceptual residence time of water in the soil and karst zone. Pleistocene aspects including quantitative and well-calibrated leaching stalagmites from Morocco show the lowest mean δ26Mg val- and precipitation experiments. ues (GDA: −4.26 ± 0.07 ‰ and HK3: −4.17 ± 0.15 ‰), and the data are well explained in terms of changes in aridity over time. The Pleistocene to Holocene stalagmites from Peru show the highest mean value of all stalagmites (NC-A and 1 Introduction NC-B δ26Mg: −3.96 ± 0.04 ‰) but only minor variations in Mg-isotope composition, which is consistent with the rather Carbon and oxygen isotope ratios as well as trace elemen- stable equatorial climate at this site. Holocene stalagmites tal abundances are widely used proxy data from speleothem from Germany (AH-1 mean δ26Mg: −4.01 ± 0.07 ‰; BU 4 archives (e.g. Genty and Massault, 1999; Spotl¨ et al., 2002; mean δ26Mg: −4.20 ± 0.10 ‰) suggest changes in outside Lachniet et al., 2004; Cruz Jr. et al., 2007; Fairchild and McMillian, 2007; Rudzka et al., 2011). The factors that Published by Copernicus Publications on behalf of the European Geosciences Union. 1850 S. Riechelmann et al.: The magnesium isotope record of cave carbonate archives control speleothem geochemistry include ambient environ- mental parameters (Baker and Genty, 1998; Spotl¨ et al., 2005; Baldini et al., 2008), carbonate mineralogy (Frisia et al., 2000, 2002; Frisia and Borsato, 2010; Wassenburg et al., 2012), as well as processes and conditions in the aquifer (Tooth and Fairchild, 2003; Miorandi et al., 2010; Sherwin and Baldini, 2011) and equilibrium and disequilibrium sta- ble isotope fractionation during carbonate precipitation in the cave (White, 2004; Tremaine et al., 2011; Riechelmann et al., 2012a). Despite significant advances in field studies (Spotl¨ et al., 2005; Asrat et al., 2008; Verheyden et al., 2008; Riechelmann et al., 2011), including experimental (Huang and Fairchild, 2001; Day and Henderson, 2011; Polag et al., 2010) and nu- merical (Muhlinghaus¨ et al., 2007; Scholz et al., 2009; De- Paolo, 2011; Dreybrodt and Scholz, 2011) work, several pa- rameters that affect proxy data remain difficult to constrain. In this respect, the validation of proxy data from individual Fig. 1. Map with the locations of studied caves. Atta and Bunker coeval stalagmites within a given cave (Dorale et al., 1998; Cave (Germany) are represented by a single green dot. Vollweiler et al., 2006; Fohlmeister et al., 2012) and between different caves (Williams et al., 2004; Mangini et al., 2005) is a key issue. 2 Case settings More recently, it has been proposed that multi-proxy stud- This study uses Mg isotope data from six stalagmites and ies including novel approaches such as fluid inclusions, noble two flowstones. These include two stalagmites from Ger- gases, clumped isotopes and non-traditional isotope systems many (Atta Cave and Bunker Cave), two stalagmites from (Kluge et al., 2008; Scheidegger et al., 2008; Immenhauser Morocco (Grotte d’Aoufous and Grotte Prison de Chien), et al., 2010; Daeron¨ et al., 2011; Reynard et al., 2011; Kluge two stalagmites from Peru (Cueva del Tigre Perdido) and two et al., 2012) may provide valuable information and comple- flowstones from Austria (Spannagel Cave). The reader is re- ment more traditional proxy data. Amongst these more re- ferred to Fig. 1 and Table 1 for detailed information regarding cently established proxies are Mg isotope (δ26Mg) data. Pre- cave parameters and speleothems investigated. vious work dealing with Mg isotope fractionation in Earth surface environments includes investigations from carbonate archives and field and laboratory precipitation experiments. 3 Magnesium isotope analyses Data available in the literature include δ26Mg values from rain, snow, riverine, soil and drip water as well as host rock Powder subsamples from longitudinally cut stalagmites and and cave carbonates and soil and cave silicate data (Galy et flowstones were dissolved in 6 M HCl. The solution was al., 2002; Young and Galy, 2004; de Villiers et al., 2005; Tip- dried and redissolved with 250 µl of a 1:1 mixture of HNO3 per et al., 2006b, 2008, 2010; Buhl et al., 2007; Brenot et (65 %) : H2O2 (31 %). Subsequently, the solution was evapo- al., 2008; Immenhauser et al., 2010; Pokrovsky et al., 2011; rated and again redissolved in 1.25 M HCl. The Mg-bearing Riechelmann et al., 2012b). Nevertheless, with the exception fraction was extracted by using ion-exchange columns (Bio- of the preliminary work shown in Buhl et al. (2007), a crit- Rad ion exchange resin AG50 W-X12, 200 to 400 mesh), ical application of the above-cited work to speleothem time evaporated to dryness and a 500 ppb Mg-solution (in 3.5 % series is lacking. HNO3) was prepared. The samples were analyzed with a Here we report on the potential and limitations of Mg Thermo Fisher Scientific Neptune MC-ICP-MS using DSM3 isotope time series proxy data interpretation from eight standard solution. The external precision was determined speleothems collected in six caves on three different conti- by measuring the mono-elemental solution Cambridge 1 nents. The goals of this study are to review parameters known against DSM3 standard solution repeatedly (n = 89, δ25Mg: to affect Mg isotope fractionation between land surface and −1.34 ± 0.03 ‰ 2σ and δ26Mg: −2.58 ± 0.06 ‰ 2σ ).
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