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Tuff ist in vielen historischen Objekten in Deutschland verbaut, hat aber wegen seiner Porosität und hygrischen Eigenschaften eine schlechte Verwitterungsresistenz. Ziel des Vorhabens ist die Entwicklung eines gesteinsmehlmodifizierten Schutzsystems auf Kieselsäurebasis (GEMOSK) zur Konservierung verbauter Tuffe. Für die Schutzmittelherstellung wird eine geeignete Mischung aus Kieselsol und feinen Gesteinsmehlen aus Steinbruchrückständen und Tuffabfällen verwendet. Bei erfolgreichem Abschluss des Projektes kann GEMOSK im Denkmalpflegebereich eingesetzt werden. Dadurch werden die Bausubstanz besser erhalten, Tuffsteinressourcen eingespart und Tuffabfälle wiederverwertet.
Stone deterioration is the result of a complex interaction of external physical, chemical and biological forces with the mineralogical-petrophysical properties of the stone. With a better understanding of how these properties are linked to material behavior and durability, more effective measures for stone conservation can be developed. Studying these interactions in tuff is particularly complex due to the naturally high heterogeneity of tuff rocks.
The first aim of a current research project is to combine the results of recent and older studies on tuff deterioration. Furthermore, the literature overview is complemented by our own investigation of Weibern and Ettringen tuff, with a focus on pore structure characteristics.
Silicon isotope fractionation during silicification is poorly understood and impedes our ability to decipher paleoenvironmental conditions from Si isotopes in ancient cherts. To investigate isotope fractionation during silica-for-carbonate replacement we analyzed the microscale Si and O isotope composition in different silica phases in a silicified zebra dolostone as well as their bulk δ18O and Δ’17O compositions. The subsequent replacement of carbonate layers is mimicked by decreasing δ18O and δ30Si. The textural relationship and magnitude of Si and O isotope fractionation is best explained by near-quantitative silica precipitation in an open system with finite Si. A Rayleigh model for silicification suggests positive Ɛ30/28Si during silicification, conforming with predictions for isotope distribution at chemical equilibrium from ab-initio models. Application of the modelled Ɛ30Si-T relationship yields silicification temperatures of approx. 50°C. To reconcile the δ18Ochert composition with these temperatures, the δ18O of the fluid must have been between -2.5 and -4 ‰, compositions for which the quartz phases fall close to the oxygen equilibrium fractionation line in three-isotope space. Diagenetic silica replacement appears to occur in O and Si isotopic equilibrium allowing reconstructions of temperatures of silicification from Si isotopes and derive the δ18O composition of the fluid – a highly desired value needed for accurate reconstructions of the temperature- and δ18O histories of the oceans.