Rensen-Pluton

The Rensen Pluton is an Oligocene , syntectonic intrusion in the eastern Alpine basement of South Tyrol . It consists mainly of granodiorite and tonalite . Together with other plutons, it forms part of the periadiatric intrusions that imposed on the border between the southern and central eastern Alps.

geography

Vals with Valler Tal to the north. The 2641 meter high Gaisjochspitze to the right above Vals is formed by the Rensen Pluton.

The elongated, east-west running intrusion , named after the 2,473 meter high Rensenspitze , is 7 kilometers long and up to 1.5 kilometers wide. It begins at the double summit of the Gaisjochspitze (2641 m) and the Gurnatschspitze or Gurnatsch (2581 m) immediately west of the Altfass valley , crosses the Valler Tal 2 kilometers north of Vals and ends at the Mutakopf (2208 m) (northeast of Mauls ) about one kilometer southwest of the Plattspitze (2669 m).

geology

The intrusion of the Rensen Pluton into the Middle Eastern Alpine Old Gneisses between the southwestern edge of the Tauern Window and the Defereggen-Antholz-Vals Lineament that passed immediately to the south took place in the Oligocene . The old gneisses are mainly composed of paragneiss , rare orthogneiss and eye gneiss , garnet mica schists from the green schist to lower amphibolite facies, amphibolites , quartzites and occasional marbles . The right- shifting Periadriatic Seam passes just 1.5 kilometers further south - the border with the Southern Alps , which is here with the Brixen Pluton . It is only 500 meters from the northern edge of the Rensen Pluton to the northern Tauern window.

The pluton runs essentially parallel to the main surface structure of the old crystalline, parts of the host rock were displaced and melted during the intrusion. This led to local assimilation and the formation of clod migmatites . A poorly developed contact zone can be observed on the northern edge of the intrusion.

At the northern contact with the old gneisses there is a steep dip to the north, at the southern edge a flatter dip of 40 to 60 ° in the same direction. The intrusion itself is divided into a tonalitic edge zone in the north and a granodioritic-tonalitic main facies in the south, which occupies 90% of the intrusion. The two types of facies can be well distinguished macroscopically. The roof of the pluton is no longer there.

Von Blanckenburg and Davies (1995) interpret the origin of the melts along the periadriatic seam and the DAV lineament as a consequence of the tearing off of the subducting masses . The magma bodies formed along the seam probably fell prey to a shear , recognizable by the partial deformation of the Oligocene intrusions such as the Bergell pluton , the Adamello pluton , the Rieserferner pluton and also the tonalitic lamellae on the northern edge of the Permian intrusions (Brixen Pluton).

Petrology

The Rensen pluton is made up of granodiorite and tonalite lithologically, the latter being particularly represented on the northern edge of the pluton. Diorite , quartz diorite , granite , monzogranite and dike rocks expand the range of variation of the otherwise relatively uniformly structured pluton. The quartz diorite forms small elongated bodies within the granodiorite and tonalite. A small mass consists of foliiertem two mica granite ( leucogranite ).

The granodiorite contains the minerals plagioclase , quartz , alkali feldspar and biotite . In addition, there are the accessories apatite , titanite , zirconium , rutile and tourmaline and the conversion products epidote , chlorite and muscovite . The tonalite has the same mineralogy, but also contains hornblende ( aluminum-iron-Tschermakit ). Rare garnet occurs in the plagioclase of quartz diorite.

The structure of the Pluton is overall hypidiomorphic and granophyric.

During contact metamorphism, skarn minerals such as wollastonite , clinozoisite , phlogopite , calcite , vesuvianite and recrystallized quartz were formed.

The magmatic events at the Rensen Pluton can be divided into four sections:

Precursors of porphyry tonalite and granodiorite. The corridors cannot be found within the main intrusion, but can extend into the Tauern window. In places they are very strongly deformed and in the immediate vicinity of the intrusion they are overprinted with contact metamorphism. Pegmatite dikes were folded isoclinally.
Main intrusion
Granite, aplite , pegmatite and quartz veins and veins . These can also be found in the pluton.
Late stage with fine-grained mafic ducts that penetrate all precursors.

Chemical composition

Main elements

For the main elements, the Rensen pluton shows the following composition:

Oxide wt.%	Diorite	Tonality	Granodiorite	granite	CIPW standard	Diorite	Tonality	Granodiorite	granite
SiO ₂	54.77	62.98	67.32	69.58	Q	8.89	20.07	25.76	34.00
TiO ₂	0.80	0.51	0.34	0.27	Or	7.12	10.41	11.80	13.75
Al ₂ O ₃	18.99	16.90	16.15	16.34	From	21.29	25.38	28.00	19.61
Fe ₂ O ₃					On	36.94	27.43	22.62	18.86
FeO	7.07 (dead)	4.59 (dead)	3.22 (dead)	3.74 (dead)	C.			0.24	3.09
MnO	0.15	0.09	0.06	0.04	Il	1.52	0.97	0.65	0.52
MgO	3.87	2.42	1.96	1.80	Mt	1.34	0.88	0.60	0.72
CaO	8.23	6.07	4.56	3.80	Hy	18.02	11.26	9.22	9.67
Na ₂ O	2.52	3.00	3.31	2.32	Tuesday	2.23	1.82
K ₂ O	1.21	1.76	2.00	2.33	Ap	0.43	0.16
P ₂ O ₅	0.19	0.07
Mg #	0.55	0.54	0.57	0.51
K ₂ O / Na ₂ O	0.48	0.59	0.60	1.00
Al / Na + K	3.49	2.47	2.12	2.58
Al / Na + K + approx	0.93	0.94	1.02	1.23
A '/ F	- 0.04	- 0.05	0.06	0.37

The Rensen pluton belongs to the calcareous rock series and shows TTG affinity . The igneous rocks are predominantly normal calcareous with a gradual fractionation trend from quartz diorite to granodiorite; However, the leucogranite is differentiated from this because it belongs to the high-K type ( English high-K-calcalkaline or HKCA for short ), recognizable by its high K ₂ O / Na ₂ O. The leukogranite has a strong resemblance to crustal rocks, which both the strontium-neodymium isotope systematics as well as inherited pragmatic components in the zircon population. It is therefore believed that it originated from crust anatexis .

The SiO ₂ content of the rocks ranges from 52 to 72 percent by weight, making them intermediate to acidic. TiO ₂ , Al ₂ O ₃ , FeO (dead), MgO, MnO and CaO are negatively correlated with SiO ₂ . Are positively correlated Na ₂ O and K ₂ O. All rocks result in CIPW standard quartz and are therefore of SiO ₂ supersaturated.

As for aluminosity , diorite and tonalite are hypoaluminos (A '/ F <0), granodiorite is normal aluminos, and leuco granite is hyperaluminos . The first three are undersaturated with aluminum or metaluminos , whereas the leucogranite is oversaturated with aluminum or peraluminos . In the standard, granodiorite and granite corundum lead , indicators of oversaturation in aluminum (pereraluminosity). In diorite and tonalite, corundum is replaced by normative diopside .

The rocks are mainly of the intrusive I-type , recognizable by Al / Na + K + Ca <1.1. Here too, the leuco granite is an exception, as it is an S-type contaminated with sediment . The K ₂ O / Na ₂ O ratio for MgO> 3 percent by weight is between 0.4 and 0.6 (with the exception of the leukogranite with 1.0), the rock samples are therefore sodium -concentrated and clearly differ from the interest rate Pluton and also from the Rieserferner Pluton , which tend more towards potassium supremacy. The magnesium numbers are between 0.51 and 0.57, typical for diorite, but quite high for granodiorite and granite.

Trace elements

Zr-Sr diagram to differentiate the rock groups of the Rensen (red) and the Rieserferner Pluton (blue). The two intrusions separate from each other, the Rensen pluton has higher zirconium contents. The arrows indicate the two trends in fractionation.

Trace element ppm	Diorite	Tonality	Granodiorite	granite
Zr	124	158	118	92
Rb	49	68	103	126
Sr	343	368	451	457
Ba	260	456	640	489

In the case of trace elements , barium , rubidium and tantalum are positively correlated with SiO ₂ , with Rb and Ta being particularly highly enriched in leucogranite. The strontium values in the Rensen pluton cover the range 340 to 600 ppm and are therefore clearly higher than in the Rieserfener pluton, whose Sr values vary between 100 and 500 ppm. They manifest an increase from diorite to granite. With similar Rb values (between 50 and 130 ppm), this results in a significantly lower Rb / Sr ratio. The main mass of Zr values varies between 90 and 160 ppm and is positively correlated with titanium (constant Ti / Zr ratio of 20).

The Zr values show a decrease from tonalite to granite. The increase in strontium with a simultaneous decrease in zirconium can be explained by a fractionation of amphibole or biotite or both together. A second development trend appears within the data volume, namely a decrease in strontium with a simultaneous decrease in zirconium. This second development trend can result from additional plagioclase fractionation.

Both development trends can also be found in the Rieserferner pluton, which is why the conclusion can be drawn that the Rensen pluton and parts of the Rieserferner intrusion have a close genetic relationship and can therefore be derived from the same or a similar melt. On the other hand, different trace element ratios show a complex, multiphase magmosetesis for both intrusives. The differences between Rieserferner and Rensen plutons can be explained either by different starting materials or by different melting rates. Higher Rb / Sr quotients for the Rieserferner complex allow magma contamination by crustal anatexis as a perfectly possible interpretation.

Isotope ratios

In the initial isotope ratios, the ⁸⁷ Sr / ⁸⁶ Sr values vary between 0.7075 and 0.7081 (quartz diorite-granodiorite), but increase abruptly to 0.7095 to 0.7110 in leukogranite. They are thus higher than the Rieserferner pluton (0.7069). The initial neodymium isotope ratios decrease from 0.51236 for quartz diorite to 0.51225 for some tonalites and leuco granite. In the neodymium-strontium diagram, the values show similarities with the Bergell pluton and the southern Adamello pluton .

In the case of lead isotopes , the rocks of the Rensen pluton manifest very homogeneous, crustal rocks comparable values - and certainly in the range of other alpine plutonites. Here, too, the leuco granite has slightly higher ratios than the diorite / tonalite at ²⁰⁷ Pb / ²⁰⁴ Pb and at ²⁰⁸ Pb / ²⁰⁴ Pb. ²⁰⁷ Pb / ²⁰⁴ Pb ranges between 15.66 and 15.68, ²⁰⁸ Pb / ²⁰⁴ Pb between 38.77 and 38.85 and ²⁰⁶ Pb / ²⁰⁴ Pb between 18.63 and 18.68. The lead values are very similar to those of the northern Adamello pluton.

Petrogenesis

Geochemistry, isotopes, and geochronology show that the Rensen pluton is not comagmatic. Its rock association is likely to be due to an intensive interaction between mafic mantle magmas and crust material. Bellieni and colleagues (1991) suggested that the petrogenesis of the Rensen pluton can best be explained by the multiple fractional crystallization of a dioritic magma under different pressures , which reacted simultaneously with the intruded crust. This created the variable strontium isotope signatures and the different trends of the compatible versus the incompatible elements.

Seated

The magma took place in two phases, as a comparison of magmatic and magnetic structural elements of the pluton with the structures in the host rock shows. During the first stage, tonalitic magma intruded with predominant north-north-east-south-south-west compressive stress, forming an east-west-oriented flattening structure, defined by regulated biotites and horn blends. In the second stage, granodioritic magma penetrated, but now in an expansion regime that was connected to the sinistral movements on the DAV lineament.

Based on Saint Blanquat and colleagues (1998), the course of the intrusion can be characterized as follows: At the beginning, the magma , which is under overpressure and active lateral shifts on the left, opened up its own intrusion zone. This in turn caused a rotation of the magmatic foliation (flattening plane compared to the compressive main stress direction) into a parallelism to the shear corridor. The initial gastric surge consisted of the amphibole-rich tonalitic peripheral facies. Thereafter, granodioritic to tonalitic magma pulses emerged, which erupted into southern areas under strain. This is indicated at least by the anisotropy of the magnetic susceptibility (AMS), the maximum intensity of which now points south, and a local deflection of the regional foliation. While the pluton was still cooling, synthetic Riedels (of the R-type) formed sinistral shear corridors, which enabled the last magma thrusts and brought the pluton closer to its current, somewhat stair-like shape. In the end, due to the rotation of the main stress axes to the northwest, late right-shifting shear zones formed, which tectonically overprinted the pluton in the low-temperature range after cooling. The last event to be mentioned is the brittle faults that gave the pluton its current shape, especially in the northeast.

tectonics

The tectonics of the Austroalpine (Middle Eastern Alpine) host rocks of the Rensen Pluton are characterized by two different kinematic deformation fields. Before the pluton penetrated, a left-shifting shear deformation running in an east-northeast direction was decisive, which had transformed the entire area around the Rensen Pluton into a sinistral shear corridor with a significant east-west extension. The shear surfaces are saiger or fall steeply to the north-north-west (with scattering in the strike from north-west to north). At the same time, they were pressed steeply to the south, triggered by the gradual emergence of the Pennine Tauern window. In addition, the side rocks were partially mylonitized by the sinistral shear . Later, porphyroblasts formed during contact metamorphosis and also the precursor ducts were still overprinted sinistrally.

The transition to transpressive, right-shifting kinematics, initiated by movements at the periadriatic suture, took place relatively quickly after the penetration of the precursor ducts and before the final solidification of the Rensen pluton. This transition from a left-shifting, ductile structure to a dextral overprinting in the low temperature range can be read from the c-axis pattern of quartz. It was accompanied by a change in the main stress directions from north-north-east to north-west and is directly related to the convergence of the European and Adriatic plate areas, which between the early Oligocene and the late Miocene (30 to 10 million years ago) were rotated counterclockwise ( cyclonic flow) had taken place. The aplit veins to the north of the massif also contain ductile structures that are overprinted by right-shifting shear sense; therefore they were deformed at the same time as the Rensen pluton.

In the late phase, antithetical, left-shifting Riedel shear surfaces (R 2), which are characterized by fine-grain quartz microstructures, as well as associated pseudotachylites . Brittle-ductile to purely brittle faults now show a north-south to north-north-west-south-south-east-directed area of tension with simultaneously occurring, east-west-directed evasive movement. The amount of the shift to the right along the Periadriatic Seam cannot be quantified, but the metamorphic Austroalpine basement was raised by 4 to 5 kilometers in the interval between 24 and 13 million years ( Chattian to Serravallian ).

In the area of the Rensen Pluton, the Austroalpine is constrained to only 4 kilometers and is dominated by left-shifting shear (with flat, east-north-east trending lineation), the intensity of which generally increases from south to north. Microstructures indicate that the grain boundary migration ( GBM ) increases in the direction of the Tauern window and thus indicates an increase in temperatures from 400 to 550 ° C. This is also the growing importance of basal sliding (English basal glide ) in the quartz in the north compared with prismatic sliding (English prism glide ) to the south, in line with those found by Mancktelow and colleagues (2001) changes the deformation mechanisms in quartz. In the south, grain lower limit rotations predominate , whereas the recrystallizations caused by grain boundary migration (GBMR processes) prevail in the north. In addition, two extremely stressed, several hundred meters wide shear corridors can be seen, one halfway between the pluton and the Periadriatic Seam (interpreted as a western extension of the DAV line) and one in the immediate vicinity of the Tauern Window. The sinistral shear was preceded by an isoclinal folding and mylonitization of tourmaline- bearing pegmatite dikes. The folds were pressed very closely together by the later shear, their axes approached the course of the elongation linear resulting from the shear and their planes tipped over to the north. Most of the time, however, only a single foliation can be seen, which is very likely the end result of several reactivations.

Low-temperature dextral lateral shifts and south-east facing shifts can be seen directly on the Rensen pluton itself and in the vicinity of the periadriatic suture. The push-ups are associated with fine-grained quartz microstructures, which lead over into the brittle area. The pluton with its ducts and veins cuts through the original sinistral shear structure and is in turn only affected by the dextral transpressive structures. This dextral overprinting can be observed particularly beautifully at the northwest contact of the Pluton south of the Plattspitze - here both the tonalite and the adjacent rock are clearly dextral sheared. The tonalite was mylonitized here at an altitude of 2550 meters and the side rock was broken up into shear band cleavage, or sbc, trending east-south-east and plunging 76 ° to the north-northeast .

Structures

Among the structures that reveal the prevailing left-shifting sense of shear in the Austro Alpin are to mention: typical SC structure , mica fish (English mica fish ), sigma clasts , sheared and rückrotierte Boudinstrukturen with their constrictions and shear bands (English shear bands ). The more or less horizontal (occasionally dipping to an angle of 30 ° to the east) lineations can be recognized by stretching linear lines made of chlorite and other mica as well as by creenulations. The pressings made steeply to the south are shown in steep isoclinally folded quartz and carbonate layers, whereby the thrust direction (hanging wall to the south) can be read from asymmetrical quartz boudins as well as from local thrusts.

Physical parameters

Krenn and colleagues determined pressures between 0.7 and 0.8 gigapascal using the Hornblende geobarometer . This corresponds to a depth of penetration of the pluton of 20 to 22 kilometers. The intrusion was thus much deeper than the neighboring Rieserferner pluton (penetration depth 12 to 15 kilometers) or the Zinsnock pluton (penetration depth 11 to 13 kilometers). The temperatures could be limited to 590 to 670 ° C by the newly formed skarn minerals in neighboring marbles during the contact metamorphosis .

Age

Borsi and colleagues had dated the Rensen pluton in 1978 to be 17 ± 4 million years ago. This corresponded to the early Miocene or Burdigalium . Using the uranium-thorium-lead system, this rather young age was revised in 1989 by Barth and colleagues to be between 31.09 ± 0.25 for quartz diorite and 31.70 ± 0.32 million years for tonalite (Oligocene, Rupelium ) . The zircons examined also contained relic ages from the early Proterozoic , as well as from the late Proterozoic and early Paleozoic .

Müller and colleagues (2000) were able to determine a precursor dike emanating from the pluton, which was mylonitized in the adjacent rock, to be 30.9 ± 0.2 million years. Ball (1989) dated less strongly deformed rhyodacitic precursor ducts to be 29.9 ± 0.5 and 29.8 ± 0.6 million years ago.

The intrusion on the Rensen Pluton can now be narrowed down to a period of 31.7 to 29.8 million years.

Individual evidence

↑ CL Rosenberg, A. Berger and SM Schmid: Observations from the floor of a granitoid pluton: inferences on the driving force of final emplacement . In: Geology . tape 23 (5) , 1995, pp. 443-44 .
^ G. Nollau: Petrographic investigations on the periadriatic reindeer granite in South Tyrol . In: Erlanger Geologische Abhandlungen . tape 98 . Erlangen 1974, p. 92 .
^ F. Von Blanckenburg and JH Davies: Slab breakoff: A model for syncollisional magmatism and tectonics in the Alps . In: Tectonics . tape 14 , 1995, pp. 120-131 .
↑ Christof Exner: The geological position of the magmatites of the Periadriatic Lineament . In: Negotiations of the Federal Geological Institute . Vienna 1976, p. 3-64 .
^ Daniel F. Stöckli: Tectonics SW of the Tauern Window (Mauls area, South Tyrol). Southern continuation of the Brenner Fault Zone and its interaction with other large fault structures . In: Diploma thesis . ETH, Zurich 1995, p. 270 .
↑ Balz Grollimund: Tectonics south of the western Tauern window (Valsertal, South Tyrol) . In: Diploma thesis . ETH, Zurich 1996, p. 173 .
↑ Reinhard Gratzer and Friedrich Koller: Variscan and Alpidic intrusions along the periadriatic seam - a geochemical comparison . In: Treatises of the Federal Geological Institute . tape 49 , 1993, pp. 137-146 .
↑ G. Bellieni G. Cavazzini, AM Fioretti, A. Peccerillo A. and G. Poli: Geochemical and isotopic evidence for crystal fractionation, AFC and crustal Anatexis in the genesis of the Rensen Plutonic Complex (Eastern Alps, Italy) . In: Contrib. Mineral. Petrol. tape 92 , 1991, pp. 21-43 .
↑ M. Saint Blanquat, B. Tikoff, C. Teyssier and JL Vigneresse: Transpressional kinematics and magmatic arcs . In: RE Holdsworth, RA Strachan and JF Dewey, Continental Transpressional and Transtensional Tectonics (Eds.): Geol. Soc. London, Special Publications . tape 135 , 1998, pp. 327-340 .
^ ^A ^b ^c Neil S. Mancktelow, Daniel F. Stöckli, Balz Grollimund, Wolfgang Müller, Bernhard Fügenschuh, Giulio Viola, Diane Seward and Igor M. Villa: The DAV and Periadriatic fault systems in the Eastern Alps south of the Tauern window . In: International Journal of Earth Sciences (Geologische Rundschau) . tape 90 , 2001, p. 593-622 .
↑ M. Stipp, H. Stünitz, R. Heilbronner and SM Schmid: The eastern Tonale fault zone: a "natural laboratory" for crystal plastic deformation of quartz over a temperature range from 250 to 700 ° C . In: Journal of Structural Geology . tape 24 , 2002, pp. 1861-1884 .
↑ D. Berhé, R. Choukroune and R. Jegouzo: Orthogneiss, mylonite and non coaxial deformation of granites: the example of the South Amorican shear zone . In: Journal of Structural Geology . tape 1 , 1979, p. 31-42 .
↑ JP Platt and RL Vissers: Extensional structures in anisotropic rocks . In: Journal of Structural Geology . tape 2 , 1980, p. 135-142 .
^ Kurt Krenn, Harald Fritz, Christian Biermeier and Robert Scholger: The Oligocene Rensen Pluton (Eastern Alps, South Tyrol): Magma emplacement and structures during plate convergence . In: Communications from the Austrian Geological Society . tape 94 , 2003, p. 9-26 .
^ S. Borsi, A. Del Moro, FP Sassi and G. Zirpolli: On the age of the periadriatic Rensen massif (Eastern Alps) . In: N. Jb.Geol.Paleont. Mh. 1978, p. 267-272 .
↑ Susanne Barth, Felix Oberli and Martin Meier: U — Th — Pb systematics of morphologically characterized zircon and allanite: a high-resolution isotopic study of the Alpine Rensen pluton (northern Italy) . In: Earth and Planetary Science Letters . Volume 95, Issues 3-4, 1989, pp. 235-254 , doi : 10.1016 / 0012-821X (89) 90100-3 .
↑ Wolfgang Müller, Neil S. Mancktelow and Martin Meier: Rb-Sr microchrons of synkinematic mica in mylonites: an example from the DAV fault of the Eastern Alps . In: Earth and Planetary Science Letters . tape 180 , 2000, pp. 385-397 .
^ T. Kugel: Geology, mineralogy and geochemistry of gangue rocks on the southwest edge of the Tauern window . In: Diploma thesis . University of Tübingen, 1989, p. 146 .

[1] CL Rosenberg, A. Berger and SM Schmid: Observations from the floor of a granitoid pluton: inferences on the driving force of final emplacement . In: Geology . tape 23 (5) , 1995, pp. 443-44 .

[2] G. Nollau: Petrographic investigations on the periadriatic reindeer granite in South Tyrol . In: Erlanger Geologische Abhandlungen . tape 98 . Erlangen 1974, p. 92 .

[3] F. Von Blanckenburg and JH Davies: Slab breakoff: A model for syncollisional magmatism and tectonics in the Alps . In: Tectonics . tape 14 , 1995, pp. 120-131 .

[4] Christof Exner: The geological position of the magmatites of the Periadriatic Lineament . In: Negotiations of the Federal Geological Institute . Vienna 1976, p. 3-64 .

[5] Daniel F. Stöckli: Tectonics SW of the Tauern Window (Mauls area, South Tyrol). Southern continuation of the Brenner Fault Zone and its interaction with other large fault structures . In: Diploma thesis . ETH, Zurich 1995, p. 270 .

[6] Balz Grollimund: Tectonics south of the western Tauern window (Valsertal, South Tyrol) . In: Diploma thesis . ETH, Zurich 1996, p. 173 .

[7] Reinhard Gratzer and Friedrich Koller: Variscan and Alpidic intrusions along the periadriatic seam - a geochemical comparison . In: Treatises of the Federal Geological Institute . tape 49 , 1993, pp. 137-146 .

[8] G. Bellieni G. Cavazzini, AM Fioretti, A. Peccerillo A. and G. Poli: Geochemical and isotopic evidence for crystal fractionation, AFC and crustal Anatexis in the genesis of the Rensen Plutonic Complex (Eastern Alps, Italy) . In: Contrib. Mineral. Petrol. tape 92 , 1991, pp. 21-43 .

[9] M. Saint Blanquat, B. Tikoff, C. Teyssier and JL Vigneresse: Transpressional kinematics and magmatic arcs . In: RE Holdsworth, RA Strachan and JF Dewey, Continental Transpressional and Transtensional Tectonics (Eds.): Geol. Soc. London, Special Publications . tape 135 , 1998, pp. 327-340 .

[Mancktelow-10] A ^b ^c Neil S. Mancktelow, Daniel F. Stöckli, Balz Grollimund, Wolfgang Müller, Bernhard Fügenschuh, Giulio Viola, Diane Seward and Igor M. Villa: The DAV and Periadriatic fault systems in the Eastern Alps south of the Tauern window . In: International Journal of Earth Sciences (Geologische Rundschau) . tape 90 , 2001, p. 593-622 .

[11] M. Stipp, H. Stünitz, R. Heilbronner and SM Schmid: The eastern Tonale fault zone: a "natural laboratory" for crystal plastic deformation of quartz over a temperature range from 250 to 700 ° C . In: Journal of Structural Geology . tape 24 , 2002, pp. 1861-1884 .

[12] D. Berhé, R. Choukroune and R. Jegouzo: Orthogneiss, mylonite and non coaxial deformation of granites: the example of the South Amorican shear zone . In: Journal of Structural Geology . tape 1 , 1979, p. 31-42 .

[13] JP Platt and RL Vissers: Extensional structures in anisotropic rocks . In: Journal of Structural Geology . tape 2 , 1980, p. 135-142 .

[14] Kurt Krenn, Harald Fritz, Christian Biermeier and Robert Scholger: The Oligocene Rensen Pluton (Eastern Alps, South Tyrol): Magma emplacement and structures during plate convergence . In: Communications from the Austrian Geological Society . tape 94 , 2003, p. 9-26 .

[15] S. Borsi, A. Del Moro, FP Sassi and G. Zirpolli: On the age of the periadriatic Rensen massif (Eastern Alps) . In: N. Jb.Geol.Paleont. Mh. 1978, p. 267-272 .

[16] Susanne Barth, Felix Oberli and Martin Meier: U — Th — Pb systematics of morphologically characterized zircon and allanite: a high-resolution isotopic study of the Alpine Rensen pluton (northern Italy) . In: Earth and Planetary Science Letters . Volume 95, Issues 3-4, 1989, pp. 235-254 , doi : 10.1016 / 0012-821X (89) 90100-3 .

[17] Wolfgang Müller, Neil S. Mancktelow and Martin Meier: Rb-Sr microchrons of synkinematic mica in mylonites: an example from the DAV fault of the Eastern Alps . In: Earth and Planetary Science Letters . tape 180 , 2000, pp. 385-397 .

[18] T. Kugel: Geology, mineralogy and geochemistry of gangue rocks on the southwest edge of the Tauern window . In: Diploma thesis . University of Tübingen, 1989, p. 146 .