The time of crystallisation ±4 Ma was determined by U Pb dating of one perfectly concordant zircon fraction. The results on other separated zircon fractions imply later radiogenic Pb loss caused by later metamorphism and exhumation of the granite and the presence of some inherited components.
Geochronology of Mórágy Granite: Results of U Pb, Rb Sr, K Ar, and 40 Ar 39 Ar isotope study
As meeting nő agee párizs follows from 40 Bár az írás flörtöl nő agee párizs 39 Ar data, K Ar system in hornblendes was disturbed with the exception of one sample that gave plateau age The difference between the U Pb zircon and the 40 Ar 39 Ar plateau ages is interpreted as a result of slow cooling of the Mórágy Granite. K Ar meeting nő agee párizs Rb Sr dating of biotites gave precise ages in a very narrow range of Ma. Quite similar age ±22 Ma was obtained by Rb Sr isochron dating of small whole-rock samples of mylonites.
These results are interpreted as pointing to the time of deformation and associated metamorphism of the Mórágy Granite. A review of the radiometric age determinations on the Mórágy Granite The geochronological study of the Mórágy Granite Figure 1 has been carried out meeting nő agee párizs the last four decades.
The results obtained are mostly K Ar, Rb Sr and Pb Pb data on the rock-forming minerals biotite, amphibole, potassium feldspar and whole-rock samples. The results were scattered between Ma biotite and Ma potassium feldspar megacrysts and whole-rock samples. The formation age of the granite was determined as around Ma. The biotite ages were interpreted in terms of a late magmatic-tectonic event which was provoked by the intrusion of the aplite dykes.
The older of the whole-rock ages was explained by the origin of the magma from Pre-Cambrian rocks whereas the younger was regarded to be a mixed age. Biotite from an aplite dyke showed an age of Ma. These Middle Carboniferous ages were related to the uplift cooling of the area. The dominant part of these ages fell into the interval of Ma.
The results can be subdivided into three groups: 1 Whole-rock ages of the granitoid rocks granodiorite syenite are scattered within a wide interval of Ma. Limiting isochrons that frame the data point cluster gave and Ma. Figure 1. Geological sketch with all historical and recent sampling points for radiometric age determinations in the Mórágy Mecsek area South-eastern Transdanubia, Hungary 1 Palaeozoic, metamorfites, 2 Palaeozoic, Mórágy granite, 3 Permian Cretaceous, mainly sedimentary rocks, 4 Cenozoic, sediments, 5 sample for radiometric measurements from outcrops, 6 sample for radiometric measurements from borehole 1.
A Mórágy Mecsek körzet földtani vázlata valamennyi irodalmi és új, radiometrikus kormeghatározásra vett minta helyzetének feltüntetésével 1 paleozoikum, metamorfitok, 2 paleozoikum, Mórágyi Gránit, 3 perm kréta, főleg üledékes kőzetek, 4 kainozoikum, üledékek, 5 radiometrikus kormeghatározásra vett minta kibúvásból, 6 radiometrikus kormeghatározásra vett minta fúrásból the last retrograde metamorphic event, whereas the older, to the beginning of the magmatism.
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Three of the nine ages for the Erdősmecske Mórágy granite ±, ± and ± Ma displayed too big analytical error, the age of the rest 6 samples varied between Ma.
In the data distribution there was a gap between and Ma. This may point to the existence of two age populations see below. The limiting isochrons resulted in and Ma. The age of 3 aplites from Erdősmecske was also Ma such as that of the country granites 2 of them is below and 1 above the age gap around Ma.
These data approximately correspond to the Rb Ar ages of the whole-rock samples of the Erdősmecske Mórágy granites 2 above and 1 below the age gap around Ma. SVINGOR and KOVÁCH concluded from the interpretation of the above data that the Mórágy Granite meeting nő agee párizs by granitisation in the following three steps: 1 the oldest igneous event occurred about Ma ago; 2 the main phase of the granitisation accompanied by intense metasomatism and leucocratic dyke formation took place around Ma; 3 tectonic activity which took place Ma ago resulted in local re-crystallisation and aplite generation in some blocks.
These ages were related to the uplift after the granitisation. These are meeting nő agee párizs younger than biotite ages, mentioned above, which was explained by later processes. For microcline Erdősmecskea K Ar age of Ma was determined which was related to the low closure temperature of this mineral. DUNKL performed fission-track FT analysis on zircon, titanite and apatite which gave information about the late thermal history of the granite body.
The FT data for zircon and titanite are old Maindicating the lack of Alpine metamorphism related to the Cretaceous orogeny. BUDA reported new age data in connection with the exploration at Üveghuta with no interpretation. They supposed a two-stage magmatic evolution elongated, prismatic zircons: ±5 Ma, tabular zircons: ±13 Ma.
Much older ages ±18 Ma were related meeting nő agee párizs the zircon crystals inherited from the Cadomian crustal fragments. The data are included into the database of following chapters of this contribution, that is why they are not discussed here in more details. Zircons originated from the granite samples of the Mórágy and Erdősmecske quarries. The older age was interpreted in terms of an early phase of the magmatic crystallisation whereas the younger age may represent emplacement intrusion of the granitoid magma.
The very old ages ~, ~, Ma of some zircon grains can be related to the presence of an inherited component originated from earlier crustal fragments. It can be concluded, that the following age intervals can be distinguished: Ma and older for leucocratic dykes; no interpretation available Rb Sr method in Hungary is not free of problems Ma for granites; the only interpretation was given by KOVÁCH, SVINGOR in terms of latest retrogade metamorphism but, again, Rb Sr method in Hungary is not free of problems Ma for granites with various centres of the data; interpretations are of two kinds: magmatic event, from the formation melting?
The idea of the metamorphic origin of the ages between Ma is the meeting nő agee párizs consistent with the recent detailed geological and tectonic observations BALLA et al. The results of these analyses are presented and discussed below.
Analytical approach General approach to dating multiple events The dating multiple events acted upon a rock is usually targeted on two goals. One is the determination of primary age of the rock; for this purpose it is useful to apply some isotope method that is proved to be reliable in distinguishing between the open and closed behaviour of an isotope system in use. The other goal is the studying of secondary ages; this approach is based on differences in the stability of different isotope systems at some conditions, and commonly utilizes several isotope methods at a time.
It was decided to study several minerals for the purpose of the detailed timing Mórágy Granite. Also, whole-rock samples of granites were studied following the classical approach of Rb Sr isochron dating of granitic magmatism FAURE Isotope methods K Ar and 40 Ar 39 Ar methods Potassium content was determined by flame photometry after acid digestion of mineral fractions.
Argon extraction and its isotope composition measurement were performed on a modified MI IG mass-spectrometer connected on line with low-blank argon extraction system.
Radiogenic 40 Ar content was determined by isotope dilution technique with 38 Ar monoisotope as a spike. The hornblende samples along with monitors were irradiated by fast neutrons. Argon extraction was carried out by step-heating method up to the C temperature. Rb Sr method All the samples were spiked by 84 Sr 85 Rb-enriched tracer prior to digestion. Prior to microwave digestion the samples were boiled in HNO 3 to dissolve sulfides. Microwave digestion was carried out at C for 20 minutes, no residue was visible after the operation.
Mineral fractions with the exception of apatite were digested in HF HNO 3 mixture at atmospheric pressure in Teflon vessels on a hot plate at C overnight. Apatite was digested in concentrated HNO 3 in Teflon vessels under the same conditions. After evaporation of the solutions, samples were dissolved in concentrated HCl and evaporated again. Next they were dissolved in 2. The columns were filled with 3. Measurements of Rb and Sr isotope compositions were carried out on a Micromass Sector 54 seven-collector mass spectrometer.
Rubidium was loaded to an outer Ta-filament of a triple-filament assembly and measured by static multicollector method.
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U Pb method Chemical dissolution of zircon was carried out in concentrated HF. The resulting solution was split into two aliquots; one was spiked by Pb U isotope tracer for determination of uranium and lead concentrations, the other one was treated unspiked for determination of lead isotope composition.
After evaporation of the solutions and conversion to an appropriate chemical form, U and Pb were extracted on microcolumns filled with BioRad AG1 8, mesh anion exchange resin. Blank level for Pb was less than 80 pg, for U, less than 20 pg. Mass discrimination during Pb and U measurements was 0.
Analyses of common lead isotope composition were carried out for correcting zircon Meeting nő agee párizs Pb data for the common lead. The isotope composition was measured with an accuracy of ±0.
All analytical errors are expressed as 2σ of the mean value except those associated with K Ar data. Samples For the purpose of dating Mórágy Granite, 23 samples of granitoids were collected from drill cores.
Ten samples represent granodiorites, five samples monzodiorites, and the rest of the collection are mylonites and one aplite. Monzodiorites differ from granodiorites not only in lower quartz and higher amphibole contents but also in optical properties pleochroism and absorption of the rock-forming biotite.
Most rocks are gneissic, re-crystallised, partially mylonitised and bear evidence of low-temperature alteration. Only few samples have retained magmatic texture and massive structure.
Other rocks have gneissic, lenslikebanded structure and composite texture combining magmatic and metamorphic blastic and cataclastic fabrics. In all those samples, crystals of magmatic minerals are deformed, partially or completely granulated, cataclased, and re-crystallised. Potassium feldspar and plagioclase occur individually while quartz aggregates and biotite flakes form nearly monomineral subparallel lenses and bands.
The gneissic and lenslike-banded textures are emphasised by the presence of fine-grained zones and bands of the same orientation which were formed during mylonitisation and subsequent blastesis, metasomatism, and hydrothermal alteration.
The newly formed metamorphic minerals epidote, secondary biotite, occasionally sericite compose a significant part of these zones. Three different sizes of samples were used in the study. Most of the samples were medium-weight, some kg; several samples has been taken as relatively large, kg pieces of core. Mylonites and aplites were sampled as very small chips of rock, less than g cut out from cores. The bigger splits of large- and medium-weight samples were sieved and separated to mineral fractions by standard electromagnetic separation and heavy-liquid technique.
Each mineral fraction was than thoroughly handpicked under a binocular microscope. During the handpicking zircon fractions were separated to morphological types on the basis of grain shape, colour, and transparency. Only large dark brown grains were picked up to avoid contamination of primary biotite by chlorite and secondary meeting nő agee párizs which is finer grained.
Biotites from least and more altered rocks differ in a degree of deformation which is not clearly seen under binocular microscope, but is easily recognised when checked in thin sections. The samples differ one from another in a degree of secondary alteration of hornblende, and Üh 23 is the least altered variety in this respect. The more altered hornblendes are partially re-crystallised and replaced by secondary chlorite. The least altered hornblende is also partially replaced by chlorite, however it is not deformed and re-crystallised.
Zircons for U Pb isotope study were separated from large samples. Two morphological varieties are mostly presented: long prismatic and short prismatic, the latter are in some cases isometric, with equally developed prism and pyramid facets. Intermediate varieties are also presented. Mineral and fluid inclusions are abundant in all types of zircon. Despite their forms, meeting nő agee párizs the grains poses signs of superimposed processes they are fractured, full of fluid inclusions along the cracks, and sometimes contain clusters of confusedly oriented inclusions which cut through growing zones.
However, grains of all the morphologic types has very good faceting and do not bear signs of re-sorption. Internal optical heterogeneity is most likely a primary magmatic growing zonation.
Analytical results Results of the K Ar dating of osztrákok flört are presented in Table 1. Isotope ages of three biotites appear to be the same within analytical errors. The age of potassium feldspar is clearly younger than that of the biotites. Step-heating 40 Ar 39 Ar study of hornblende samples Table 2 has revealed complex distribution of ages obtained for different gas fractions.
Hornblende Üh 18 is characterised by a smooth down-ladder structure of age spectrum Figure 2, a. Sample Üh 27, unlike the former, Table 1. K Ar isotope dating data for minerals from Mórágy granitoids has age spectrum that is more like up-ladder Figure 2, c meeting nő agee párizs, although it also has a fraction of high-temperature gas with rather young age.
Age spectrum of Üh 31A hornblende is very similar to a U-shape with surprisingly old over Ma last high-temperature step Figure 2, d. Both mineral isochrons for the samples Figure 3, a, b are characterised by excessive scatter of analytical points. Although the isochron lines go straight through the biotite points, other minerals do not fit the lines.
The point labels on the diagram are some times bigger than analytical errors, so deviation from the isochrons for some of the points is times larger than the errors. For the sample Üh 22A egyedülálló anyák ismerkedés Rb Sr age is For the sample Üh 22B mineral isochron gives Rb Sr age of Notable is meeting nő agee párizs both Rb Sr ages are indistinguishable within their uncertainties.
No simple regularity can be observed in the analytical point scatter. Rb Sr isotope results for whole-rock samples are presented in Table 4 and on an isochron diagram at Figure 3, c.
Distribution of the analytical points is very complex to approximate the whole set by a common line. At least three groups of points and respective lines can be distinguished. Within analytical errors the first two age estimations are indistinguishable.
Common lead isotope composition was determined in feldspars from five heavy-weight samples Table 5. The data meeting nő agee párizs obtained for both plagioclase and potassium feldspar from each sample, with the exception of sample Üh 31A, for which only potassium feldspar was analysed. Lead isotope composition in coexisting feldspars of a given sample are markedly different. Table Ar 39 Ar stepwise heating data for hornblendes from Mórágy granitoids Figure 2.
Hornblende 40 Ar 39 Ar age spectrums for Mórágy granitoids a granodiorite Üh 18 m ; b granodiorite Üh 23 m ; c granodiorite Üh 27 m ; d granodiorite Üh 31A m. Rectangular height represents ±2σ error of a step age 2. A Mórágyi Gránit amfiboljának 40 Ar 39 Ar korspektrumai.
Rb Sr isotope data for mineral fractions of Mórágy granitoids Figure 3.
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A Mórágyi Gránit egyes ásványfrakcióinak és teljeskőzet-mintáinak Rb Sr izokróndiagramjai. Table 5. Lead isotope composition in feldspars from Mórágy granitoids Analytical error for all presented isotope ratios is less than 0. Table 6. U Pb zircon isotope data for Mórágy meeting nő agee párizs 1 In cases of selective dissolution L stands for leachate and R for restite 2 All isotopic ratios are corrected for blank 80 pg for Pb and 20 pg for U and 0.
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U Pb zircon isotope data are presented in Table 6. For each sample, at least two zircon fractions were analysed. All the data were corrected for common lead isotope composition determined by analysis of potassium feldspar. Sample Üh 18 Figure 4, a. Three zircon points are equally discordant and quite far from upper intercept of a discordia and concordia at ± Ma. Although the discordia MSWD value of 2. Flört op het werk Üh 18A Figure 4, b.
Four zircon points do not fit any common line and are equally discordant. No age estimation is possible.