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Notes: Abstract In the attempt to study the composition and behaviour of metasomatically active solutions we have examined the kind of gaseous solutions which are formed by water in contact with the minerals of a granite under a pressure of 2000 bars at 600° C, and how these solutions behave within a temperature gradient at the same pressure. The temperature ranged from 620° to 180° C. The following minerals were considered: quartz, K-feldspar (adularia), plagioclase (andesine) and mixtures of quartz with adularia, quartz with andesine, quartz with adularia and andesine, quartz mixed with mierokline-perthite, oligoelase and biotite. All these minerals are completely dissolved by water under these physical conditions. The solutions always contain more silica than the minerals, if quartz is present. The dissolved components are transported within the temperature gradient. In the solutions, Ca derived from the anorthite-component of the plagioclase and Mg from the biotite form associations together with silica, which travel tohigher temperatures. There they crystallize in form of wollastonite and/or diopside. On the other hand, Na and K, AI and the Fe from the biotite and the largest part of the silica, travel from the 600° C-region tolower temperatures. There they crystallize in form of quartz, K-feldspar, albite, some muscovite and Mg-free biotite rich in Fe. In experiments of only short duration, metastable analcime instead of albite has been formed. In long lasting experiments of 10 weeks, a separation of Na and K was evident: Albite was formed in the temperature range 470° to 420° C, whereas K-feldspar (with some albite component) and Mg-free biotite crystallize together with quartz in a larger temperature range below 420° C; see figure 6. The different minerals from a mixture influence each other's solubility in such a way that the amount of both feldspars and quartz dissolved and transported within a unit of time is decreased. Compared with the amount obtained when quartz alone constitutes the solid phase, only 40 % of that amount is dissolved and transported when the quartz had been mixed with adularia; the value amounts to only 30% when it was mixed with andesine. When both feldspars. are present together with quartz, the amount of dissolved and transported quartz is decreased to about 20 % of the original amount; see table 7. However, in all cases the amount of dissolved quartz is larger than the sum of the dissolved feldspar substances. Thus, the solution formed from a mixture of quartz and feldspars which is transported to lower temperatures always contains more silica than the mineral mixture. The amount of adularia dissolved and transported is reduced by the presence of quartz to 1/6 of that amount furnished at 6000 C by adularia alone. Under the same conditions the amount of andesine is reduced to one half. — The amount of adularia transported per unit of time is nearly equal to the amount of plagioclase components if quartz is present. However, if no quartz is present, the proportion of dissolved and transported adularia to plagioclase-components is noticeably shifted in favour of adularia. This would be the case with syenite as the source for the solutions. In the attempt to produce skarns in a way closely related to nature, silica-rich solutions from a granite have been brought into contact with dolomite. The contact was situated at 600°, 570° and 500° C. With equal duration of the experiments, the results were similar. With different durations the following effect was observed: at the beginning, the silica-rich solution reacts with the dolomite under formation of forsterite, calcite and C02. When more materialis transported into the contact,region diopside (the mineral containing more silica) is formed from calcite, forsterite and additional silica. When the same metasomatically active solution meets a marble, (contact at 600° C) wollastonite is formed. In these metasomatic processes the partial pressure of C02 in the gasphase remained low under our experimental conditions.

Notes: Abstract The equilibrium curves for the reactions: (a) 4 orthozoisite + 1 quartz ⇌ 5 anorthite + 1 grossularite + 2 H2O. (b) epidote (+ quartz) ⇌ anorthite + grossularite/andradite + haematite + H2O (+ quartz) have been worked out. Both reactions were reversed in the presence of seeds. Without seeds no stable equilibrium could be achieved, because of the sluggish nucleation of epidote and orthozoisite. From the starting oxide mixtures anorthite and garnet have been formed at all experimental conditions, and from these epidote or orthozoisite, respectively, have been crystallized in their stability fields. The experiments showed, that both epidote and orthozoisite can form at lower pressures than have hitherto been repor ted. Epidote will form at H2O-pressures 1000–2000 bars lower (at temperatures up to 600° C) than are needed for the formation of orthozoisite. This explains, why epidotes are observed much more frequently than orthozoisite in the outer zone of contact-metamorphism. Other petrographic observations like the presence of orthozoisite and the absence of epidote in some high grade metamorphic rocks can be well understood from the different course of the respective equilibrium curves. Some equilibrium data for the orthozoisite- and the epidotereaction, respectively, are given below: