Rieserferner Pluton

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View from Fenneregg (3123 m) over Barmer Spitze (3200 m) to the Hochgall (3436 m) and the eastern Rieserferner with the snowy Nock (3358 m). The Hochgall, the highest mountain in the Rieserferner group, consists of fine-grained tonalite. The contact between the bright pluton and its darker metamorphic enveloping rocks can be clearly seen on the right edge of the picture.

The Rieserferner Pluton , in Italian Plutone delle Vedrette di Ries , is an Oligocene intrusion in the eastern alpine basement of East and 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, but differs in its extremely elongated shape. The Rieserferner Pluton is named after the Rieserferner group .

geography

The position of the Rieserferner Pluton (red) south of the Tauern window is easy to see.

The Rieserferner Pluton, the third largest of the periadriatic intrusions, lies immediately north of the Defereggen-Antholz-Vals Lineaments (DAV Lineaments), a significant sinistral lateral displacement associated with the periadriatic suture . The southern edge of the Tauern window is only about 5 to 10 kilometers further north. The intrusion is over 40 kilometers long and 4.5 to a maximum of 7 kilometers wide. Its longitudinal axis follows the east-west direction and runs more or less parallel to the DAV lineament. With a vertical exposure of 2500 meters from floor to roof, the Rieserferner intrusion is one of the world's most open-minded plutons.

The main intrusion begins in the west in the Tauferer Tal immediately east of Sand in Taufers and ends in the east near Sankt Jakob in Defereggen . From here, its thin tail continues to the southwest of Hopfgarten in Defereggen .

geology

Geological map of the Tauern Window and its frame. The Rieserferner-Pluton (dark red) with the Hochgall is located about 25 kilometers southwest of Matrei in East Tyrol .

During the Oligocene and Miocene , the Eastern Alps (and thus also the area of ​​the Rieserferner Pluton) were affected by an intensive, north-south-directed narrowing. This was accompanied by an expansion running parallel to the strike of the orogen, which was to culminate in a crust extrusion to the east. This compressive tectonic regime is also responsible for the formation of the Tauern Window - a gigantic bulge structure, which on both its western and its eastern edge was caused by shallow faults that occurred during the narrowing (the Brenner fault in the west and the Katschberg fault in the East) is cut off. The lateral evacuation movement was taken up by conjugate lateral shifts, for example by the right-shifting periadriatic suture or the left-shifting Salzachtal-Ennstal-Mariazell-Puchberg lineament (SEMP lineament). Widespread east-west trending stretch lines and fold axes in the host rocks of the Rieserferner intrusion document this orogen-parallel expansion.

The intrusion had occurred in the Middle Oligocene into the Greenschist Facial, Central Eastern Alpine Old Gneisses south of the Tauern Window. Their north contact shows a shallow dip to the north under the old gneiss, the south contact to the DAV lineament is directed steeply to the south. The intrusion consists of two large core areas, the Rieserkern in the east and the Rainwaldkern in the west. In the middle area of ​​the intrusion between the two cores, the so-called old roof - the roof region of the pluton - is still preserved. The framework rocks of the intrusion are mica schist and amphibolite , which were overprinted by contact metamorphosis . The eastern section in Defereggental , which runs roughly parallel to the DAV lineament, is tail-shaped and does not become much wider than 100 meters.

The intrusion-related heating resulted in the formation of new minerals of andalusite , sillimanite , garnet , staurolite and, more rarely, cordierite .

The magmatism along the Periadriatic Seam can be divided into three sections: a north-east-south-west facing west section, in which the plutons intrude into the southern Alps and reach the border of the overturned Austroalpine continental crust. The magmatism manifests itself in small plutons, volcanic coverings and andesitic dikes with high potassium content. In the central section, the periadriatic magmatism reached its highest development with the Adamello pluton , which penetrated the southern Alpine basement with its Permomesozoic cover layers, and with the Bergell pluton , which took place in five alpine nappes - including crystalline Penninic , ophiolites and Austroalpine crust . In the eastern section, the magmatism is concentrated in the Austroalpine. In the southern Alps only smaller occurrences can be found. Most of the plutons in this section are elongated, oriented in an east-west direction and thus document their penetration during active lateral shifts along the periadriatic suture and its side strands. The Rieserferner pluton represents the largest intrusion of the eastern section and is accompanied a little further south by the smaller Zinsnock pluton . Other intrusions are the Rensen pluton and the Altberg pluton .

Spatial structure

Wildgall , 3273 meters, seen from the southeast. To the right of the Hochgall , 3436 meters. Steep conveying zone of the intrusion.

The spatial structure of the Rieserferner Pluton can be reconstructed very well on the basis of the post-intrusive tilt, which uncovered over 2000 meters with excellent exposure conditions. The roof of the Pluton (old roof) occupies several tens of square kilometers in the central part of the intrusion and on its northern edge. The floor appears at the west end. The foliation shows that the intrusion dips slightly to the north, but that it dips more and more steeply to the south as it approaches the DAV. The intrusion-internal contact between the fine-grained and coarse-grained tonalite facies in the slightly dipping northern part is more or less flat.

The spatial arrangement of the foliations and a contour map of the contact with the metamorphic adjacent rock show that the roof of the pluton consists of two dome structures, which are separated by a trough-shaped saddle. The axis plane of this trough strikes in a north-south direction and thus runs perpendicular to all structures in the adjacent rock. Such an arrangement can actually only be explained by the active penetration of the tonalite and not by a regional deformation.

The southern edge of the intrusion, like the foliation of the adjacent rock and the spatial position of the DAV, plunges steeply to the south. In places it can be observed how the magmatic structure runs parallel to the DAV mylonites and therefore suggests a simultaneity between intrusion and mylonitic deformation.

Within this zone with steep foliation, decimal to hectometric concentric areas can be seen, in which the magmatic linear also plunge steeply. Such structures do not occur in other parts of the pluton or in the adjacent rock. The spatial connection of these structures with the steep zone in the Pluton suggests that these are ascent channels of the intrusion. The tonalitic magma had thus risen in the southern part of the intrusion in the immediate vicinity of the DAV line with its mylonites. Because of the later tilting, the tail-shaped eastern part of the intrusion, which extends the steep zone to the east, represents a structurally higher level of the coast compared to the main part; it is therefore seen as an extension of the ascent zone towards the hanging wall, which possibly supplied other plutons in the upper crust with magma (for example, a connection between the Rieserferner pluton and the Zinsnock pluton was considered for a long time).

Physical parameters

According to Cesare (1992), the minimum penetration depth of the Rieserferner Pluton is given as 9 kilometers on the basis of progressive contact metamorphosis data. This corresponds to a pressure of 0.29 gigapascals . However, a penetration depth of 12 to 15 kilometers (corresponding to a pressure of around 0.5 GPa) can still be regarded as quite realistic. Tajcmanová and colleagues (2009) found a pressure of 0.41 GPa, corresponding to a penetration depth of around 15 kilometers. Compared to the other periadriatic intrusives, the Rieserferner pluton was therefore a rather deep-seated intrusion. On the host rocks at the edge of the intrusion, 600 to 620 ° C could be determined, corresponding to a pressure of 0.25 GPa. The magma itself should have had a temperature of 800 to 760 ° C.

Petrology

Petrography

View from Fernerköpfl (3248 m) to the Schneebigen Nock (3358 m). It's nice to see the contact between the lighter tonality of the Rieserferner intrusion in the foreground and the old roof - darker, amphibolite-faced gneisses on the Schneebigen Nock.

The intrusion of the Rieserferner Pluton took place in three magma bursts, which can be separated from one another petrologically and geochemically. The first magma pulse was coarse-grained and mainly filled the west dome (rainforest core), the north edge of the intrusion and parts of the south edge. Its composition varies from diorite (52.5 to 54.3 percent by weight SiO 2 ) to granodiorite (63.3 to 70.6 percent by weight SiO 2 ), with tonalite (58.5 to 66.5 percent by weight SiO 2 ) predominating. Granite (70.4 to 79.0 percent by weight SiO 2 ) is rare. The second batch is medium to fine-grained and consists of tonalite to granite. The rock members show spatial mixing ( English mingling ). The third pulse is also medium to fine-grained and concentrates on the central (Rieserkern) and eastern part of the intrusion. Its composition is very homogeneous and consists of a leukogranodiorite.

In the pluton, the granodiorites clearly predominate, which, like the tonalites, have a hypidiomorphic grainy texture. The granites and diorites form irregularly distributed small masses within the intrusive body. The pluton also contains mafic inclusions and inclusions of the metamorphic shell rocks and is also crossed by aplites and lamprophyren . The mafic microgranular inclusions (English mafic microgranular enclaves or MME ) are common, especially in the first magma surge. They are likely to represent mafic magma bubbles that have been geochemically altered through contact with the host magma, easily recognizable in reaction zones. The metamorphic inclusions are not only found (as expected) at the edge of the intrusion, but also inside. Small mica-rich xenolites are particularly common in the second gastric surge. The assimilation of the adjacent rocks must therefore have played an important role in the magma development, as the broad geochemical composition and the rather high strontium isotope initial ratio make clear.

In the late stage of the intrusion all Petrofazies were of mafic and acidic passages interspersed. The thickness of the acid passages is in the centimeter to meter range. They mostly run in an east-west direction and can form swarms, which, however, only rarely penetrate the metamorphic bedrock. The last igneous formations were aplites and pegmatites, whereby aplites predominate and can lead to spessartine as garnet . Lamprophyre dikes show a predominant north-south orientation, their contacts to the host rocks are often razor-sharp.

The mafic veins are in the centimeter to decimeter range and do not belong to the Rieserferner cycle, as they penetrate both the plutonic rocks, including the aplites and pegmatites, and the metamorphic neighboring rocks. They are younger than the main intrusion and have a fairly variable chemistry, ranging from trachy basalt to basaltic andesite. They belong to either the calcareous or the Shoshonite series. These late Andesite dikes occur not only in the Austroalpine, but also in the Southern Alps and the Penninic. They have been dated by Steenken and colleagues (2000) to be 26.3 ± 3.0 million years old (Upper Oligocene, Chattian ).

mineralogy

Gelttalspitze (3126 m) from the northeast. It is built up from the fine-grain tonalite facies. Immediately behind it is the metamorphic series of envelopes with the eastern foothills of the Black Wall (3105 m) on the right, which plunges steeply to the south towards the DAV lineament .

The general modal mineral inventory of the Rieserferner Pluton is made up of the following minerals :

The granodiorites consist of clearly zoned plagioclase (An 60-90 ), quartz, alkali feldspar and biotite. Hornblende, clinozoisite , zirconium , apatite and ilmenite are to be cited as accessories . The tonalites have a very similar mineral composition, only the volume fraction of zoned plagioclase is slightly higher in them. In addition, they do not have a hornblende. Garnet was observed in tonalites in the contact area of ​​the intrusive body. The granites are essentially composed of quartz, alkali feldspar and plagioclase with the accessory phases apatite, zirconium and orthite . The diorites consist mainly of hornblende and zoned plagioclase (An 50-80 ) as well as subordinate biotite, quartz and garnet.

Chemical composition

The following table is intended to illustrate the geochemical composition of the main elements of the Rieserferner pluton:

Oxide
wt.%		 Mafischer
inclusion		 Diorite Tonality Granodiorite granite
SiO 2 57.32 53.38 62.69 67.30 73.01
TiO 2 0.77 0.90 0.60 0.40 0.15
Al 2 O 3 16.82 18.59 17.28 16.23 14.39
Fe 2 O 3
FeO 8.08 (dead) 8.07 (dead) 4.80 (dead) 3.31 (dead) 1.40 (dead)
MnO 0.22 0.22 0.11 0.09 0.05
MgO 3.76 3.94 2.27 1.34 0.37
CaO 6.58 7.66 5.47 3.99 2.19
Na 2 O 2.54 2.57 2.87 3.13 3.19
K 2 O 2.45 2.00 2.41 3.17 4.43
P 2 O 5 0.22 0.23 0.14 0.13 0.07
TAS diagram with the compositions of the sub-alkaline Rieserferner intrusion (brown crosses), the alkaline Karawanken granite pluton (red crosses) and the sub-alkaline Karawanken tonalite pluton (blue crosses). All three igneous rows are clearly separated from each other, only the tonalites of the Rieserferner intrusion and the Karawanken tonalite pluton are similar.

The intrusives of the Rieserferner Pluton are sub-alkaline and, in particular, calcium-alkaline magmatites of the high-K type. Their SiO 2 content fluctuates between 53 and 73 percent by weight, so the rocks are intermediate to acidic. They are also characterized by a very low TiO 2 content, which is below 0.9 percent by weight. The Al 2 O 3 concentration is increased, but its ratio FeO / MgO is low.

All rock members are quartz-normative and with a few exceptions (especially with the diorites, but also with some tonalites and granodiorites) also corundum- normative. They are therefore all oversaturated with SiO 2 and mostly peraluminous or even just metaluminous.

The three magma pulses can be clearly separated from one another geochemically based on the content of calcium , strontium and rubidium . Using the trace elements , two further rock groups can be characterized whose normalized ratio Tb N / Yb N is either below 1.1 or above.

Bellieni and colleagues (1981) take the view that the three magma series of the Riesserferner pluton developed in two steps from a common parent magma by means of crystal-enamel fractionation . The first phase proceeded under high pressure, hornblende and garnet were fractionated and thereby magmas high Tb N / Yb N emerged. With their further ascent under now decreasing pressure, a second fractionation phase occurred - this time, however, hornblende and instead of garnet plagioclase were separated, which depleted the magma composition of strontium. Contamination with crust material and the separation of accessories were then decisive for the increased ratio of 87 Sr / 86 Sr and for the uneven distribution of trace elements.

Petrogenesis

Beautiful sharp contact between the pluton and its resting old roof on Roßhorn (3068 m).

The magma origin of the Rieserferner pluton and other plutons along the Periadriatic Seam has been the subject of controversy for a long time. For a long time, the Andesitic magmas were considered to be the late Upper Oocene phase of subduction magmatism. Geochemical results support this view. Alternative ideas are melting through crust expansion or the crustal melting of the mountain root after the alpine lithospheric root had been reduced in thickness by convection currents. Due to the isotope distributions and the spatial arrangement of the plutons along the periadriatic seam, von Blankenburg and Davis (1995 and 1996) endorsed the hypothesis of a slab break-off (tearing off of the subducting plate).

tectonics

The left-shifting DAV lineament is a branch of the periadriatic seam and runs along the southern edge of the Rieserferner pluton. It accompanies the tail-like eastern part of the pluton immediately southwards, but then turns from the middle part of the intrusion to the southwest and then flows into the Periadriatic Seam after about 30 kilometers. The lineament divides the basement into a north and a south half, with the south half remaining untouched by the alpine metamorphosis. The wedge-shaped northern half with the Rieserferner pluton was affected by two deformations - Da1 and Da2 . The second deformation Da2 took place at the same time as the mylonite formation along the DAV lineament and the placement of the granitoids of the Rieserferner pluton.

As with other east-north-east trending shear zones on the western Tauern window, left-shifting sense of shear indicators can be identified on the DAV lineament. Together with east-south-east to south-east trending, but right-shifting shear zones further east, a conjugate shear zone system was created which accommodated the forced east-west stretching during the bulging of the Tauern window due to the north-south-directed narrowing. These observations, together with the sinistral shear sense along the DAV lineament and the synclinal folding immediately north of it, indicate a generally transpressive deformation field.

Structures

The structures within the Rieserferner Pluton are directly related to both the cooling magma and the simultaneous tectonic movements on the DAV lineament. So husband and Scheuvens could (1998) based mikrotektonischer identify studies that after solidification of plutonic rock a grünschieferfazielle deformation had followed an originally magmatic to submagmatische deformation. The latter solid body deformation can in turn be divided into a high and a low temperature range.

Magmatic / submagmatic deformation

An igneous foliation is defined in the pluton by the linear arrangement of platy plagioclase ridges. The Albitz twins are aligned parallel to her. Together with undeformed biotite packages, plagioclase forms a weak SPO structure ( shape preferred orientation ), ie the two crystals occupy preferred spatial positions because of their external shape. The plaster-like appearance of biotite (English tiling ), which overlaps with plagioclase like roof tiles, indicates a non-coaxial flow structure .

Fractures in the plagioclase are characteristic of the submagmatic stage, which have been filled in with residual melt that is still present and are now present as a mixture of quartz and alkali feldspar. Allanite is also affected by submagmatic fractures. Quartz shows indolent extinction and a checkerboard pattern. The latter indicate a temperature of 600 to 700 ° C and the transition to solid body deformation. The edges of the quartz grains are also bulged and refer to a clear grain boundary migration by recrystallization (English grain boundary migration Recrystallization or GBMR ).

High temperature solid body deformation

Microstructures of the high-temperature solid deformation manifest themselves mainly in quartz and biotite. In quartz, checkerboard patterns and GBMR can still be seen, flattened quartz grains are now emerging, which develop into quartz ribbons, lined with a border of fine sub-grains . With increasing solid deformation, the biotite loses its homogeneous grain size distribution, kink bands appear and sawtooth-like growth limits indicate recrystallization. In the high temperature range, basal sliding becomes more and more important with falling temperatures with biotite and a coherent intracrystalline weak layer ( IWL ) is created in combination with recrystallized quartz around the plagioclase structure . The feldspars are not yet recrystallized and only heavily deformed specimens show a rather indistinct, indolent extinction. However, some bent twin lamellas clearly show deformation.

The occurrence of myrmecite , which sits on corroded microcline crystals (recognizable by the crossed twins), indicates a temperature of around 550 ° C and thus indicates metasomatic processes, is significant.

Low temperature solid body deformation

With a further decrease in temperatures, typical C / S structures developed from the intracistalline weak zones (IWL) , which macroscopically correspond to mylonites and quartz mylonites . Biotite mostly retrograded to chlorite (probably with the help of hydrothermal fluids). Shear sense indicators such as biotite fish or inclined quartz foils show a predominantly left-shifting sense of shear. The quartz crystals are characterized by very clear, undolute extinction and undersize grain boundaries. Grain boundary migration at low temperatures can be recognized by the noticeable bulges .

Mylonitic south-east trending dextral lateral shifts affect the northern margin and particularly the eastern process of the intrusion, the latter being sheared and nearly boudinated. The southern edge along the DAV line is also traversed by analogous mylonitic side shifts, which strike more east-south-east.

Brittle deformation

After leaving the ductile area, the Rieserferner pluton was deformed brittle. The brittle deformation is particularly evident under the microscope on broken quartz. Macroscopically emerged in the cooled rock now upheavals , cataclasites and crevices . Pseudotachylites also occur in association with the cataclasites .

Distribution of the structures in the pluton

Igneous structures are only preserved in the western rainforest core, solid deformation is found in the central Rieser core and in the eastern extension. With the exception of a left-shifting mylonitic zone (with the most intense solid deformation) on the northern edge of the Rieserkerne, the solid deformation generally increases to the south and east.

Seat of the Pluton

The ascent and taking place of the Rieserferner Pluton took place in several stages. At the beginning, the ascent of the melt took place parallel to the steep foliation on the DAV Lineament, an active mylonitic shear zone. The final emplacement can be divided into two further steps, due to the attenuation by hydraulic fracture Zerrbrüche (English extensional hydrofracturing ) in the surrounding host rock just north of Mylonitgürtels was a tabular Magmenkörper in the form of a powerful bearing passage north penetrate into the neighboring rock. In the storage corridor wedge, the magma then expanded and bulged, deforming the roof area above it into dome-like structures. After the intrusion activity subsided, the entire pluton was tilted 2200 meters to the east (which corresponds to a rotation angle of 5 °) due to non-coaxial tectonic constraining movements ( indentation tectonics ), so that the west side of the intrusion was now more pronounced and eroded as well Due to erosion, lower structural levels and even the floor of the magma chamber in the west were released.

Age

Using rubidium-strontium dating, Borsi and colleagues (1979) were able to determine an intrusion age of 30 ± 3 million years for the Rieserferner pluton (Upper Oligocene, Rupelian ). Müller and colleagues (2000) obtained the age of formation of mylonites along the DAV lineament between 33 and 30 million years. This age is comparable to a crystallization age of 32.4 ± 0.4 million years, which Romer and Siegesmund (2003) determined on Allanite.

See also

literature

  • Diethard Mager: Geological map of the Rieserferner group between Magerstein and Windschar (South Tyrol). In: The Sciliar . tape 59 , 1985, pp. 358-379 .

Individual evidence

  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. 443-446 .
  2. ↑ a b R. Kleinschrodt: Quartz grain structure analysis in the old crystalline south of the western Tauern window (South Tyrol / Italy) . In: Erlanger Geologische Abhandlungen . tape 114 , 1987, pp. 1-82 .
  3. ↑ NS Mancktelow include: The DAV and the Periadriatic fault system in the eastern Alps south of the Tauern window . In: International Journal of Earth Sciences . tape 90 , 2001, p. 593-622 , doi : 10.1007 / s005310000190 .
  4. ^ B. Cesare, AM Fioretti and C. Rosenberg: The periadriatic intrusion of Vedrette di Ries - Rieserferner (Eastern Alps): Petrology, emplacement mechanisms and contact aureole . In: 32nd International Geological Congress, Field Trip Guide Book . Volume n ° 2 - B17, 2004, p. 1-32 .
  5. ^ A b 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 .
  6. ^ Friedrich Becke : Petrographic studies on the tonalite of the Rieserferner . In: Tschermaks Min. Petr. Mitt. Band 13 , 1892, p. 379-464 .
  7. ^ W. Prochaska: The contact center of the Rieserfernerintrusion in East and South Tyrol . In: Dissertation at the University of Vienna . 1980, p. 88 .
  8. ^ GV Dal Piaz and G. Venturelli: Brevi riflessioni sul magmatismo post-ofiolitico nel quadro dell'evoluzione spazio-temporale delle Alpi . In: Memorie Società Geologica Italiana . tape 26 , 1983, pp. 5-19 .
  9. ^ A b c André Steenken, Siegfried Siegesmund, Till Heinrichs and Bernhard Fügenschuh: Cooling and exhumation of the Rieserferner Pluton (Eastern Alps, Italy / Austria) . In: International Journal of Earth Sciences . tape 91 , 2002, p. 799-817 , doi : 10.1007 / s00531-002-0260-4 .
  10. ^ B. Cesare: Metamorfismo di contatto di rocce pelitiche nell 'aureola di Vedrette di Ries (Alpi Orientali - Italia) . In: Atti Ticinesi di Scienze della Terra . tape 35 , 1992, pp. 1-7 .
  11. ↑ L. Tajcmanová, JAD Connolly and B. Cesare: A thermodynamic model for titanium and ferric iron solution in biotite . In: Journal of Metamorphic Geology . tape 27 , 2009, p. 153-165 .
  12. ↑ a b 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, ISBN 3-900312-85-0 , pp. 137-146 .
  13. ↑ G. Bellieni, G. Cavazzini, AM Fioretti, A. Peccerillo, G. Poli and P. Zantedeschi: Petrology and geochemistry of microgranular mafic enclaves from the Vedrette di Ries plutonic complex (Eastern Alps) . In: Per. Mineral. tape 58, 1-3 , 1989, pp. 45-65 .
  14. ^ S. Borsi, A. Del Moro, FP Sassi and G. Zirpoli: On the age of the Vedrette di Ries (Rieserferner) massif and its geodynamic significance . In: Geologische Rundschau . tape 68 , 1979, pp. 41-60 .
  15. ↑ GO Gatto, A. Gregnanin, GM Molin, EM Piccirillo and A. Scolari A .: Le manifestazioni Andesitiche polifasiche dell'Alto Adige occidentale nel quadro geodinamico alpino . In: St. Trentin. Sc. Nat. tape 53 , 1976, p. 21-47 .
  16. ^ André Steenken, Siegfried Siegesmund and Till Heinrichs: The emplacement of the Rieserferner Pluton (Eastern Alps, Tyrol): constraints from field observations, magnetic fabrics and microstructures . In: Journal of Structural Geology . tape 22 , 2000, pp. 1855-1873 .
  17. ↑ G. Bellieni: Caratteri geochimici del massiccio granodioritico-tonalitico delle Vedrette di Ries (Rieserferner) -Alto Adige Orientale . In: Rend. Soc. It. Miner. Petr. tape 34 , 1978, p. 527-548 .
  18. ↑ G. Bellieni A. Peccerillo and G. Poli: The Vedrette di Ries (Vedrette) Plutonic Complex: Petro Logical and Geochemical Data Bearing on Its Genesis . In: Contrib. Mineral. Petrol. tape 78 , 1981, p. 145-156 .
  19. ↑ FP Sassi, G. Bellieni A. Peccerillo and G. Poli: Some constraints on the Geodynamic models in the Eastern Alps . In: New Yearbook for Geology and Paleontology . Monthly booklets 1980, 1980, p. 541-548 .
  20. ↑ H. Kagami, P. Ulmer, W. Hansmann, V. Dietrich and RH Steiger: Nd-Sr isotopic and geochemical characteristics of the southern Adamello (northern Italy) intrusives: implications for crustal versus mantle origin . In: Journal of Geophysical Research . tape 96 , 1991, pp. 14331-14346 .
  21. ^ Hans Peter Laubscher : The late Alpine (Periadriatic) intrusions and the Insubric Line . In: Memorie della Societa Geologica Italiana . tape 26 , 1983, pp. 21-30 .
  22. ↑ JF Dewey: Extensional collaps of orogens . In: Tectonics . tape 7 , 1988, pp. 1123-1139 .
  23. ^ F. von Blanckenburg and JH Davis: Slab breakoff: a model for syncollisional magmatism and tectonics in the Alps . In: Tectonic . tape 14 , 1995, pp. 120-131 .
  24. ↑ a b W. Müller, NS Mancktelow and M. Meier, M .: 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 , doi : 10.1016 / S0012-821X (00) 00167-9 .
  25. ↑ D. Mager: Geological and petrographic investigations on the southern edge of the Rieserferner Pluton, taking into account the intrusion mechanism . In: Doctoral thesis at the Friedrich Alexander University . Erlangen-Nuremberg 1985, p. 182 .
  26. ↑ H.-G. Linzer et al: Balancing orogenic float of the Eastern Alps . In: Tectonophysics . tape 354 , 2002, pp. 211-237 , doi : 10.1016 / S0040-1951 (02) 00337-2 .
  27. ↑ MR Handy et al .: Mechanical coupling, decoupling and strain partitioning during transpression along the Periadriatic Fault System (European Alps) . In: D. Gapais, J.-P. Brun and PR Cobbold, Deformation Mechanisms, Rheology and Tectonics: From Minerals to the Lithosphere (Eds.): Geological Society [London] Special Publication . tape 243 , 2005, pp. 249-276 .
  28. ↑ A. husband and D. Scheuvens: Structural investigation of the northern contact of the Rieserferner Plutonic Complex (Eastern Alps) - first results. In: Terra Nostra. Writings of the Alfred Wegener Foundation . tape 98 , 1998, pp. 62 .
  29. ^ WD Means and Y. Park: New experimental approach to understanding igneous texture . In: Geology . tape 22 , 1994, pp. 323-326 .
  30. ↑ IR Tribe and RS D'Lemos: Significance of a hiatus in down-temperature fabric development within syntectonic quartz diorite complexes, Channel Islands, UK . In: Journal of the Geological Society of London . tape 153 (1) , 1996, S. 127-138 .
  31. ↑ Ralph Wagner, Claudio L. Rosenberg and Mark R. Handy: Fracture-driven intrusion and upwelling of a mid-crustal pluton fed from a transpressive shear zone — The Rieserferner Pluton (Eastern Alps) . In: Geological Society of America Bulletin . 118, no. 1/2, 2006, p. 219-237 , doi : 10.1130 / B25842.1 .
  32. ^ S. Borsi, A. Del Moro, FP Sassi and G. Zirpoli, G .: On the age of the Vedrette di Ries (Rieserferner) massif and its geodynamic significance . In: Geologische Rundschau . tape 68 , 1979, pp. 441-60 .
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