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Interactions between dioritic and granodioritic magmas in mingling zones: plagioclase record of mixing, mingling and subsolidus interactions in the Gęsiniec Intrusion, NE Bohemian Massif, SW Poland

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Abstract

Dioritic and granodioritic rocks coexist in the Gęsiniec Intrusion in SW Poland showing typical relationships in many mafic–felsic mingling zones worldwide, such as dioritic syn-putonic dykes and microgranular enclaves within granodioritic host. Plagioclase zonation from granodioritic rocks suggests late stage mixing probably with dioritic magma, whereas no magma mixing is recorded in plagioclase from dioritic rocks. The diorites seem to show effects of interaction with evolved, leucocratic melts derived from granodiorite, not with the granodioritic melt itself. We conclude that the diorites’ compositions were modified after their emplacement within the granodioritic host, when the diorites were essentially solidified and injection of evolved melt from granodiorite did not involve marked modification of plagioclase composition. Compositional zoning patterns of plagioclase in diorites can be modeled by closed system fractional crystallization interrupted by resorption induced probably by decompression. Granodioritic plagioclase seems to be affected by the same resorption event. Plagioclase that crystallized in dioritic magma before the resorption does not record interaction between dioritic and granodioritic magmas, suggesting that both magmas evolved separately.

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Acknowledgments

The research work was supported by grants to AP: 2022/W/ING/07 and KOLUMB by the Polish Science Foundation. We are grateful to Vojtech Janoušek and Bill Collins for very helpful reviews and editorial comments. Chris Hawkesworth is thanked for valuable comments on an early version of this manuscript, and his suggestions as to how the English might be improved.

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Correspondence to Anna Pietranik.

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Communicated by B. Collins.

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Appendix

Calculation of Sr content in melt from Sr plagioclase composition allows for interpreting the change of Sr concentration in plagioclase in terms of contemporaneous change of melt composition. However, despite the obvious appeal of this approach, it requires certain assumptions to be made. They are discussed below:

Recalculation of Sr content in plagioclase to Sr content in the melt from which the plagioclase crystallized assumes equilibrium partitioning between crystal and melt. The equilibrium is not reached if the rate of crystallization is controlled by diffusion of elements to the crystal surface. However, such a kinetic control on crystallization should lead to either oscillatory zoning (e.g., Sibley et al. 1976) or skeletal morphology of plagioclase (Lofgren 1980), none of which is observed in diorites and only some oscillatory zoning occurs in outer parts of granodiorite plagioclase (Pietranik et al. 2006). Also consistent trends in An versus Sr in the melt plot observed for all rocks suggest that the change of Sr concentration in plagioclase is probably reflecting the actual change in melt composition. However, if recalculated Sr content in the melt represents true melt composition, then the value for the first plagioclase to crystallize (probably that with the highest An content) should be close to or higher than the whole rock Sr content since the plagioclase is the only high-temperature phase that concentrates Sr. For that statement to be true requires that the whole rock represents magma composition; however, there is no structural or geochemical reason to expect that the most mafic dioritic rocks are cumulates or hybrid mixtures of minerals derived from different magmas, as will be shown in this paper. The offsets between Sr whole rock content and Sr content in the melt in equilibrium with the cores of plagioclase are ~130 ppm for granodiorite GD15 and ~50–70 ppm for diorite. The offsets are slightly higher than propagated error on Bindeman et al. (1998) equation RT ln D Sr = aX An + b (1SD = ~30 ppm), where D Sr = C plag/C melt (C x-concentration of Sr in phase x) assuming individual errors on C plag, T and X An are 90 ppm, 100°C and 1 mol%, respectively. If errors on a and b coefficients are taken into account the propagated error is ~180 ppm, therefore, almost completely overlapping with the range of results for granodiorite and diorite. However, only C plag and X An should contribute to the scatter of the data, whereas changes in T, a and b would increase or decrease calculated C melt of whole set of data. Therefore, we accept that the calculated C melt is only accurate within error ~180 ppm; however precision of the data and thus trends observed in An versus Sr diagram is much better ~30 ppm and can be interpreted as a change of melt composition contemporaneous with plagioclase crystallization.

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Pietranik, A., Koepke, J. Interactions between dioritic and granodioritic magmas in mingling zones: plagioclase record of mixing, mingling and subsolidus interactions in the Gęsiniec Intrusion, NE Bohemian Massif, SW Poland. Contrib Mineral Petrol 158, 17–36 (2009). https://doi.org/10.1007/s00410-008-0368-z

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