Lower Engadine window

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Geological sketch of the Engadine window

The Lower Engadine Window or Engadine Window is a tectonic window of the Alps in the Lower Engadine area ( Graubünden ) and the Upper Court ( Tyrol ) landscape adjoining the valley . Surrounded by Eastern Alpine blankets , a distance of approx. 55 km along the Inn Valley, Penninic ceilings and sheds exposed.

Corresponding to the course of the Inn, which essentially created the window, it has an oval shape stretched in SW-NE direction. Its southwest end is near Giarsun , the northeast near Prutz . In between it is up to 17 km wide. It is roughly in equal parts in Switzerland and Austria ; the two parts were therefore explored using different approaches in the past.

Geological importance

The Lower Engadine Window is a key area of ​​Alpine geology:

  • The Lower Engadine window, like the Rechnitz window , the Tauern window and the Gargellen window about 20 km to the north-west, play a major role in researching the architectural style of the Alps. Here, the deeper subsoil comes to light , which is covered almost everywhere else in the Eastern Alps by the tectonic blankets of the Eastern Alps.
    The window-like outcrops of deeper structural units under the framing Eastern Alpine ceilings here and in the Tauern window were the first indications in 1903 of lateral or sub-horizontal transport of rock masses over greater distances: it was to be assumed that the higher ceilings were pushed over the lower ones; by forces from the interior of the earth that were still unknown at the time.
  • Due to the great thickness of the Graubünden slate opened up here and its particularly monotonous development, structural changes can be followed excellently: These include the spatial position of the slate surfaces, the orientation of folds of different ages, the stretching lineation marked by deformed minerals and others.
    As a result, the course of the mountain deformation could first be specified and then, for the first time in the Alps, an extensive correlation between the movements of lithospheric plates and alpine structural units (here the ceilings and scales of the window) could be demonstrated.
    Similarities between the directions, the sense of rotation and the angles of rotation of the forces acting from outside and the movements inside the alpine nappes over around 75 Ma (period from the Upper Cretaceous to the Upper Miocene) were recognized. These results have refuted the western motion model of the Alpine kinematics, which was previously considered valid.

The Inntal vault

Structure of the alpine earth crust in the area of ​​the Engadine window (after Hitz & Pfiffner 1994, graphically modified).
The Inntal vault is only visible in the upper 10 to 12 km of the crust. Any existing SE part of the vault, which may have been lowered by the Engadine fault, is missing.
As = Arosa zone, Tasna = Tasna zone, Conrad = Conrad discontinuity . Below SK coordinates of the profile ends and the profile kink in the date CH1903.

Even if the Inn and its tributaries as well as the Ice Age Inn glacier have removed the higher Eastern Alpine ceilings in the area of ​​the window, the Pennine structural units have only been exposed because a curvature of the Alpine earth crust has moved the lower surfaces of the Eastern Alpine ceilings upwards, i.e. into the area of ​​impact of erosion. The associated vault structure is called the Inntal vault.

The vault (= the area of ​​relative elevation of the lower ceiling surfaces ). is larger than the Pennine area exposed by erosion (= Engadine window and side window ). The middle of the Inntal vault is probably in the middle of the Engadine window, for example in the Piz Mundin area. However, it has its highest point in the area from Pfunds to Lafairs in the narrow northeast part of the window. There the vault has steep sides and plunges steeply towards the northeast. Towards the southwest, the ceilings plunge more gently, as do the flanks of the vault in the southwest.

Like the window, the vault also has a longitudinal southwest-northeast running direction. Several parallel "waves" of the ceiling undersurface can be seen ( anticlinorium ). This is the reason for the ragged window edge in the gently sloping south-west of the vault. The pop-ups, “exclaves” and “enclaves” of the window have their own names. From the Inn near Giarsun follow north:

  • Half window by Giarsun
  • Half window of Val Tuoi
  • Half-window of Urezzas
  • Breitwassertal half-window
  • Laraintal half-window (2 pieces)

Between the half-windows there are half-cliffs (flaps of the Silvretta ceiling). Within the area of ​​the Silvretta ceiling and approx. 3 km outside the Engadine window, on the northwest flank of the Inntal vault, is the small ...

  • Jamtal window

Within the area of ​​the Engadine Window, there are also two cliffs of the Silvretta ceiling in hollows of the Inntal vault :

  • Paulcketurm cliff
  • Larain cliff

Beyond the Engadine Fault , the Inntal anticlinorium presumably continues in the large folds of the Scarl blanket to the southeast.

The Inntal vault should not pause through the entire regional earth crust. According to evaluations of seismic profiles within the framework of NRP20 , it appears to be only laid out in the Eastern Alpine and Pennine floors, while the lower Helvetic floor forms a stack of crustal scales. The only slightly deformed part of the European crust follows even deeper. The deformation is greatest in the higher floors, whereby the Penninic rocks with their overall low shear strength made it possible to decouple the movements between the upper floors and the Helvetic floor. The additional compression then led to the formation of the vault in the area above the shed stack.

Mountain construction in the Engadine window

Tectonic map sketch of the Engadine window and its surroundings

overview

In the Engadine window, the Penninic, which was run over by the Eastern Alps and then buried underneath it until the Young Tertiary, was exposed again. The initially uniform Eastern Alpine thrust mass is now in 3 layers:

  • Silvretta Nappe, with normal thrust contact with the Penninic
  • Scarl-Nappe (also S-charl-Nappe), broken down into the Engadine line, therefore with largely preserved sediment layer
  • Ötztal ceiling, pushed onto the exposed window and all neighboring building units in a late phase of movement

The Penninic and its oceanic or continental base is present in several blankets or scale zones (also: tectonometamorphic zones ). In addition to the Penninic building units, Eastern Alpine sheds are exposed directly under the Silvretta ceiling. Follow from tectonically higher to tectonically lower:

  • Subsilvrettide miners, Flimjoch wedge
  • Fimber zone (including Arosa zone)
  • Tasna zone
  • Zone of Rots-Pezid
  • Pfundser Zone

The term 'zone' in the Engadine window reflects the difficulty and uncertainty of geological exploration. He originally meant a sedimentary zone, i.e. H. an elongated outcrop in which the rocks differ from the lying and the hanging wall petrographically, without a real stratigraphy being able to be established. When, in the course of time, the ceiling and shed construction in the window was recognized, the concept of zone was retained and was reinterpreted tectonically. It now means 'shed zone', i.e. H. an elongated outcrop made up of scales from the same deposit space. If the offset between the sheds is small compared to the offset of the entire shed zone against the lying and hanging zones, then one can speak of a ceiling. That applies to the Pfundser Zone.

By submerging the flanks of the Inn Valley vault to NW and SE as well as the vault axis to NE and SW, the erosion created an onion-shell-shaped arrangement of these structural units. However, not all units occur around the window frame; some wedge out, others are cut off from the Engadine fault, others covered by the Ötztal cover (see below tectonic development ). Basically, all of the building units that are unlocked in the window continue under the framing Eastern Alpine ceilings until they wedge out.

Other structural units in a similar or the same tectonic position reappear in the east in the Tauern window, in the west in the Gargellen window and in the Prättigau half window, from where the Penninic-Eastern Alpine contact can be traced south to the Bernina Alps. The northern edge of the Silvretta Nappe is the thrust contact with the nappes of the Northern Limestone Alps ; accordingly, no Penninic comes to light here, but only again at faults within the Limestone Alps and on their northern edge. The connection between the Penninic, which is exposed in the Prättigau, the Inn Valley and the Hohe Tauern, is impressively documented by the geomagnetic evidence of the ophiolites typical of the Penninic under the Silvretta Nappe and under the Ötztal Nappe. It is therefore clear that the units described below from the bottom up are not necessarily related to the Engadine window: you are just open-minded there!

Pfundser Zone

Name: After the centrally located village of Pfunds , developed from the older term Pfunds series , which emphasizes stratigraphic peculiarities and does not yet reflect the tectonic character of this building unit. Since the discovery of a structurally distinguishable core and that of its high pressure metamorphosis, the Pfundser Zone has also been divided into the lower Mundin Nappe and the higher Arina Nappe (or Arina Pfunds Nappe).

Three groups of rocks make up the unit: ophiolites , Bündnerschiefer and eastern alpine clods.

The ophiolites include tholeiitic pillow lavas , basalts , basalt ducts, breccias of pillow lavas, hyaloclastites and isolated radiolarites . The thickness cannot be specified exactly, but is far more than 100 meters. Due to geochemical criteria, they are considered to be the oceanic crust of the Valais trough. The period from Callovium to Cenomanium is generally used as the educational age .

The deepest exposed rocks of the window are the Bündner slate of the Pfundser zone. Ophiolites are again to be suspected among these, because the sequence ophiolite - Bündner schist is repeated several times on tectonically higher floors of the shed zone. The sequence of the Bündner slate on top of the ophiolites is classically divided into three parts. A more recent attempt at structuring comes from Bertle (2004). The connection with the classic structure is only clear for the colorful Bündner schist (see table):

Classical structure of the Bündner slate
(from hanging to lying)
Structure of the Bündner slate according to Bertle 2004
(from hanging to lying)
Colorful Bündner slate Malmurainza Formation (> 100 m; Turbidite ; Upper Cretaceous)
Saderer Joch series

basal gray Bündner slate
Fuorcla-d'Alp-Formation (approx. 10 m; formed in an oceanic-anoxic event ; Albium )
Gault formation (approx. 40 m; flyschoide, sandy-clayey sequence; Aptium / Albium)
Tristel formation (approx. 30 m; turbiditic; Barremium / Aptium)
Limestone schist (approx. 20 m; at the base Tuffite; Neokom)

Due to the isoclinal fold construction found on Piz Mundin with tilted storage and reduplications, Bertle also estimates the thicknesses previously set at 1500 to 2000 meters to be only around 500 meters.

In the absence of fossils, the slates are difficult to date; for the deposition of the gray Bündner schist, however, the period from Dogger to Campanium is assumed (later than the ophiolites). The Saderer Joch series comes from the Maastrichtian , dated using orbitoids . The colorful Bündner schists then reach into the Eocene . In the Bündner schists there are several clods of eastern Alpine facies with Triassic ages.

The slate surfaces form a north-east-south-west trending anticline , or an anticlinorium, similar to that of the Inntal vault. However, the angle of inclination of the slate anticline depicts the vault only indirectly, the slate anticline is an epiphenomenon of the Inntal vault.

In the middle of their axial culmination, the Bündner schists reach epizonal degrees of metamorphosis (high pressure-low temperature metamorphosis, HP / LT - lower green schist facies with new formation of actinolite , carpholite and pumpellyite ). In addition to crossite and lawsonite, the metabasalts of the ophiolites even show bluish slate facial overprinting based on glaucoma . The metamorphosis reached pressures between 1.1 and 1.3 GPa in the lower section of the Pfundser Zone (Mundin Unit), corresponding to a depth of approximately 30 to 35 kilometers, at a temperature of 350 to 375 ° C. In the higher areas (Arina unit) the metamorphic conditions weakened to 0.6 GPa and 300 ° C. It is not known whether the central gneisses known in the Tauern window with overlying high-rise marble still exist among the Bündner schists .

The Pfundser zone is tectonically overlaid by the Rots-Pezid zone.

Zone of Rots-Pezid

Name: The unit has been delimited differently in the course of research and given numerous names. Zone von Roz-Champatsch-Pezid and Zone von Champatsch are still partly in use , whereby the name component Champatsch comes from the ophiolites of Alp Champatsch, which were formerly included in this zone (near Scuol ). They were separated from the lying Bündner slates in 1941 and added to the newly erected Ramosch shed in 1972 (see below Tasna zone). The component Roz comes from an older spelling of today's Piz Rots near Samnaun .

There is a prospecting zone at the lying boundary of the unit. Old crystalline, quartzite and carbonates from the Triassic (crystalline limestone, clay-marly slate and dolomite), marbles from Jura and Chalk , ophiolites (with tristle layers and Gault ) and Cretaceous flysch are mixed together like scales . The mining zone shows affinities to the wildflysch of the Feuerstätter ceiling .

The sub-eastern Alpine sheds on the Stammerspitz , Frudiger and Burgschrofen also belong to this tectonic level . As hardships, they each form distinctive peaks. The sequence begins at the Stammerspitz with the main Triassic dolomite and Kössen layers , followed by colorful lias and breccias in the Jura , then marl , quartzite, radiolarite and finally aptych layers . Due to a facial relationship, the scale is interpreted as an extension of the Err-Bernina Nappe.

The actual Roz-Pezid zone joins the prospecting zone, which is also severely disturbed. It forms a schisty-sandy-calcareous sequence of 200 to 1000 meters in thickness . The zone contains gray Bündner slate with underlying colored Bündner slate and clayey equivalents of the Tristle layers and the Gault and is interpreted as a low metamorphic flysch.

The Rots-Pezid zone is overlaid by the Tasna zone.

Tasna zone

Name after the occurrence around the Val Tasna (Silvretta group).

The Central Penninic Tasna Zone begins with the ophiolite- rich Ramoscher Zone in the southwest, which merges into the Prutzer Zone to the northeast . The Ramoscher Zone contains phyllonitized old crystalline, which may have emerged from the Paleozoic Era , followed by the rudimentary Permomesozoic Era , consisting of Ladis quartzite (Lower Triassic), dolomite lenses and Bunter Keuper with gypsum . It probably originates from an intrapennine threshold area. The associated ophiolite masses with magnesite veins , nickel ore and copper enrichments are problematic in such an interpretation, unless the Ramoscher zone represents the immediate transition area from the continental facies (Briançonnais) to the oceanic facies of the Valais trough. The ophiolite masses consist mainly of serpentinitized peridotite with associated Ophicalcites and serpentinite breccias. Lenticular metagabbros are found in and near the peridotite.

The Prutzer Zone contains secured Paleozoic Era, composed of quartz phyllite and iron dolomite with pale ore , copper gravel and arsenic gravel . This is followed by quite mighty Ladis quartzite, fossil-bearing Triassic rocks as well as gray and colored Bündner slate.

The very differently structured Tasna blanket pushes itself over the Ramoscher zone . At its base it has the Tasna granite , a green (due to chloritization ), epimetamorphic granite gneiss that also occurs in the Falknis cover and in the Sulzfluh cover . Normally about these crystalline base unit of continental origin follows a scantily educated Permotrias with Kristallinbrekzien and rhyolites , transgredierendem Hauptdolomit , quartzite Keuper with gypsum and colored shales, fossil-rich Steinberger Lias and Falknisbrekzien, then pelagic limestones from the Middle Jurassic and finally Malmkalke . Furthermore Cretaceous follow Neokomschiefer , Tristelschichten with Orbitoliniden , powerful sandstones of the Gault (at Piz Tasna ), glauconite -Quarzite, only a few meters thick expectant quartz - sandstones , gray marl and Couches Rouges with Globotruncanen from the Upper Cretaceous. Paleogene flysch forms the end of the Tasna Nappe. The Tasna Nappe was metamorphosed under the conditions of the lower greenschist facies.

Fimber zone

Name after the Fimbertal, which separates the Samnaun group from the Silvretta group.

The fimber zone (including the Arosa zone ) leads in association with various flyschen ( Idalpsandstein from the Dogger , possible flysche from the Malm, the Neokom and the Aptium , as well as Höllentalflysch from the Cenomanium / Turonium ) Tasna prospectors. It also represents a strongly deformed tectonic mixing zone, which consists of Triassic dolomites, quartzites, radiolarites , black schists from the Hauterivium / Aptian and in particular ophiolites (which are missing in the underlying Tasna cover). The Idalp ophiolite series is made up of serpentinites , gabbros , diabase and basalts from the South Penninic Ocean. It shows a double metamorphosis: an oceanic high temperature metamorphosis and a later high pressure metamorphosis. The high pressure metamorphosis took place at pressures between 0.7 and 0.9 GPa and temperatures of around 250 ° C (transition from the green slate to the blue slate facies).

The intensive tectonization of the fimber zone is based on the pre-Gosau (before the Coniacium ) crossing of the Silvretta crystalline .

Subsilvrettide miners, Flimjoch wedge

Under the actual Silvretta ceiling there is still a perforated carpet of Middle Eastern Alpine clods of tracks. These are Triassic and crystalline clods that can be several kilometers wide. The diggers occur exclusively along the Silvretta Thrust, i.e. where the thrust contact has remained without later complications. They reappear on the western edge of the Silvretta ceiling against the Prättigau half-window, where they are given the local name 'Madrisa-Schollen'.

The miners of eastern alpine facies and the crystalline shavings - like the Flimjoch wedge - are probably the forehead scales of the Silvretta crystalline that were run over; A lower-eastern alpine origin is also debatable.

Eastern Alpine frame

The Pennine ceiling stack in the Lower Engadine window is run over from the east and south by the Silvretta ceiling , which forms the western and northern part of the frame. Along its base it occasionally shows pseudotachylite ducts - evidence of the frictional heat released during the thrust processes. The eastern window frame is formed by the huge Ötztal ceiling , which slid along the Schlinig thrust in WSW direction over the Silvretta ceiling and the Engadine Dolomites. Because of these conditions, Bruno Sander already referred to the Lower Engadine window as a scissor window . In the north-east there are Permomesozoic sediments as a frame, which were injected at the Thial-Puschlin fault between the Silvretta blanket and the phyllite gneiss zone following to the north.

Engadine lineament

On its south-east side, the window is cut off by a supraregional disturbance , the Engadin disturbance (also Engadin Lineament or Engadin Line ). This is a sinistral lateral shift , which at the same time raised the north-west side of the window, so that on the south-east side the rock sequences above the Bündner schist are partially mutilated (e.g. the Tasna zone) or are absent (the zone is missing von Rots-Pezid).

Tectonic evolution

The tectonic development of the Lower Engadine Window can be explained in connection with the thrust of the Eastern Alpine over the three-part Penninic sedimentation area. Relative movements occur in northeast, northern, northwest and westerly directions.

Already towards the end of the Lower Cretaceous in the Upper Barremium / Aptian around 125 to 120 million years ago, the transition from a passive to an active continental margin occurred in the Eastern Alps . The first movements of over travel Austroalpine and Subduktionsvorgänge can be in the Albian , the Cenomanian and Turonian distinguish the turonische phase of the aforementioned vorgosauischen phase corresponds. The East Alpine sediments and their crystalline underlay were sheared off and developed into the East Alpine nappes. In the area of ​​what is now the Engadine Window, this led to the gradual formation of the Silvretta , Scarl and Ötztal ceilings and an accretion wedge at their feet. This accretion wedge was the forerunner of the tectonometamorphic zones opened up inside the window.

The palaeogeographical arrangement of these zones is reflected in their current spatial arrangement in the pile of nappes: The southern Penninic fimber zone (with the Arosa zone) as the most southern unit lies directly below the Eastern Alpine, below that follows the threshold area of ​​the Tasna zone further north (northernmost foothills of the central Penninic Briançonnais) and at the bottom the northernmost northern Penninic zones of Rots-Pezid and Pfunds, which come from the Valais trough.

During the time of the Gosau (in the Campanian ) the southern Penninic sedimentation area (fimber zone) is swallowed up and the Eastern Alps undergoes a first metamorphosis ( Eo-alpine metamorphosis around 110 to 90 million years ago, with cooling ages up to 65 million years). Between the Upper Campanian and the Paleocene there was probably an isostatic uplift of the accretion wedge that was forming, indicated by the suspension of marine Gosau sedimentation in Carinthia . During the Paleocene and Eocene, the pile of nappes then advanced into the North Pennine and even the Helvetic sedimentation area and ended the accretion process. The enormous load led to a rise in temperature and caused a metamorphosis of the lower green schist facies in the Penninic of the window interior during the Upper Eocene, the Oligocene and the Lower Miocene (actual alpine metamorphosis in the period 38 to 16 million years BP, with a thermal maximum around 30 million years). Of course, the lower-lying Pfundser zone was most severely affected (Mundin unit).

The alpine metamorphosis was followed by the general lifting and further cooling of the orogen, documented by means of radiometric age determinations on light mica and crack age on zirconium and apatite .

This did not end the narrowing of the Eastern Alps, however; instead, subduction and accretion shifted to the northern edge of the Alps. In this context, the Inntal vault was also built in the period 10 to 5 million years BP (Upper Miocene). The actual erosive formation of the window began at the latest in the Messinian (Sarmatian) around 7 million years ago, as the base of the Silvretta ceiling was first cut by the Inn during this time (pseudotachylites from the ceiling base were detected as pebbles in the Chiemgau molasse ). From the Pliocene onwards , the area around the Lower Engadine window is subject to isostatic compensatory movements.

The left-shifting Engadine lineament became effective in the Rupelium 30 million years ago at the earliest , as evidenced by the offset of the contact aureole around the Bergeller Pluton .

View towards ONO into Hintergamor and into the Val di Gastei (left) from the area of ​​the Norberthöhe (digital terrain model with geological map).
3 nappes can be seen, separated by 2 faults: on the right the Ötztal nappes in bright colors, under the Schlinig thrust the trapped remainder of the Scarl nappes, consisting of the so-called upper gneiss range (purple red) and overlying dolomite (light blue). On the NW side of the Engadine Fault, the Bündnerschist (gray) and metabasalts (green) of the Pfundser zone.
The Schlinig Thrust and the steep Engadine Fault meet in the Hintergamor; then the latter disappears under the Ötztal cover. This means that the edge of the Engadine window in the background that continues to NE is clearly the Schliniger Thrust and that the thrust movement in its final phase is even younger than the Engadine Fault.

In a further late phase, a transverse, west-facing thrust of the Ötztal Nappe over the Silvretta Nappe and Scarl Nappe (Schlinig thrust ) took place on the upper floor . However, this movement also had an effect on units in the eastern part of the window interior and must therefore have taken place after the bulge in the Upper Miocene (however, much older Middle Cretaceous and Paleogenic movements are also known at this fault area, and it is said to have been effective as a detachment of the expansion tectonics be).

Individual evidence

  1. P. Termier: Les nappes of Alpes orientales et la synthèse des Alpes. In: Bull. Soc. géol. France. 4th sér., T. III, Paris 1903, pp. 711-765. (to the Engadine window on p. 748.)
  2. ^ P. Termier: Sur la fenêtre de la Basse-Engadine. In: Comp. rend. Acad. Sci. 139, Paris 1904, pp. 648-650.
  3. H. Förster, CR Mattmüller: Kinematic concept of the Adriatic-Eurasia movement. In: Jb. Geol. B.-A. 140/1, Vienna 1997, pp. 51-71.
  4. ^ CR Mattmüller: Geometric investigation of the Inntal vault. In: Jb. Geol. B.-A. 139, Vienna 1996, pp. 45-69.
  5. L. Hitz, OA Pfiffner: Interpretation of Line E3: The deep structure of the Engadine Window. In: L. Hitz: Crustal structure at the transition between central and eastern Alps: processing, 3D modeling and interpretation of a network of deep seismic profiles. Diss. Univ. Bern 1994, pp. 48-62.
  6. ^ H. Heinz, W. Seiberl: Magnetic structures of the Eastern Alps west of the Tauern window. In: Mém. Soc. géol. France. ns 156, Paris 1990, pp. 123-128.
  7. R. Oberhauser: The Lower Engadine Window. In: Geol. B.-A. (Ed.): The geological structure of Austria. Vienna 1980, pp. 291-299.
  8. ^ CR Mattmüller: Structures of the Engadine Window. Volume I: Tectonics and Kinematics. Volume II: Appendices. Diss. TH Aachen 1999, DNB 958895449 .
  9. ^ R. Bousquet, R. Oberhänsli, B. Goffé, L. Jolivet, O. Vidal: High-pressure-low-temperature metamorphism and deformation in the Bündnerschiefer of the Engadine window: implications for the regional evolution of the eastern Central Alps. In: J. metamorph. Geol. 16/5, Oxford 1998, pp. 657-674.
  10. ^ SB Dürr et al .: Geochemistry and geodynamic significance of the north Penninic ophiolites from the Central Alps. In: Switzerland. Mineral. Petrogr. Mitt. 73, 1993, pp. 407-419.
  11. ^ R. Bousquet et al .: The tectono-metamorphic history of the Valaisan domain from the Western to the Central Alps: new constraints on the evolution of the Alps . In: Geol. Soc. Amer. Bull . tape 114 , 2002, pp. 207-225 .
  12. J. Cadisch et al: Geological Atlas of Switzerland. 1: 25000, No. 14 / sheet 420 Ardez <Siegfried Atlas>, explanations. Ed .: Geol. Komm. Schweiz. Naturf. Ges. Bern 1941.
  13. R. Trümpy: On the geology of the Lower Engadine. Ecological investigations in the Lower Engadine. 4th result scientific research Swiss. Nat.park XII, Chur 1972, pp. 71-87.
  14. L. Kläy: Geology of the stem tip . In: Eclog. Geol. Helv. Band 50 , 1957, pp. 323-467 .
  15. D. Florineth, N. Froitzheim: Transition from continental to oceanic basement in the Tasna nappe (Engadine Window, Graubünden, Switzerland): evidence for Early Cretaceous opening of the Valais ocean . In: Switzerland. mineral. petrogr. Mitt. Band 74 , 1994, pp. 437-478 .
  16. D. Vuichard: The ophiolitic suite of the Alp Champatsch (Lower Engadine Window, Switzerland): the metamorphic and tectonic evolution of a small oceanic basin in the Penninic realm? In: Ofioliti . tape 9 , 1984, pp. 619-632 .
  17. ^ AF Waibel, W. Frisch: The Lower Engadine Window: sediment deposition and accretion in relation to the plate-tectonic evolution of the Eastern Alps . In: Tectonophysics . tape 162 , 1989, pp. 229-241 .
  18. A. Tollmann: The Lower Engadine Window. In: Geology of Austria. Volume I, Vienna 1977, pp. 76-83.
  19. ^ U. Ring et al.: The internal structure of the Arosa Zone (Swiss-Austrian Alps) . In: Geol. Rundschau . tape 79 , 1990, pp. 725-739 .
  20. ^ V. Höck, F. Koller: The Idalp Ophiolite (Lower Engadine Window, Eastern Alps): Petrology and Geochemistry . In: Ofioliti . tape 12 , 1987, pp. 179-192 .
  21. M. Thöni: A review of geochronological data from the Eastern Alps . In: Switzerland. Mineral. Petrogr. Mitt. Band 79/1 . Zurich 1999, p. 209-230 .
  22. F. v. Blankenburg et al .: Time calibration of a PT-path from the Western Tauern Window, Eastern Alps. The problem of closure temperatures . In: Contrib. Mineral. Petrol . tape 101 , 1989, pp. 1-11 .
  23. Fügenschuh include: Exhumation in a convergent orogen. The western Tauern Window . In: Terra Nova . tape 9 , 1998, pp. 213-217 .
  24. H. Wieseneder in H. Graul: Gravel analytical investigations in the Upper German Tertiary hill country. With a rubble petrographic section by Hans Wieseneder . In: Dep. Bayer. Akad. Wiss., Math.-nat. Abt., NF 46, Munich 1939.

literature

  • Rufus J. Bertle: The Sedimentary Record of North Penninic Schistes lustrés of the Lower Engadine Window and its Correlation to the Tauern Window (Eastern Alps) . 2004 ( online version; PDF file; 694 kB ).
  • Hans Egger among other things: Geological map of Austria 1: 1,500,000 . ( Online version; PDF file; 1.6 MB ( Memento from September 7, 2012 in the Internet Archive )).
  • Manfred P. Gwinner: Geology of the Alps . E. Schweitzerbart'sche Verlagbuchhandlung, Stuttgart 1971, ISBN 3-510-65015-8 .
  • Roderich Mattmüller: Considerations about the ceiling kinematics in the Engadine window . 1991 ( online version; PDF file; 807 kB ).
  • R. Oberhauser, FK Bauer: The geological structure of Austria . Springer, 1980, ISBN 3-211-81556-2 , pp. 110, 291 ( main chapter from page 291 f. In the Google book search).
  • Dieter Richter: Outline of the geology of the Alps . Walter de Gruyter & Co., Berlin / New York 1973, ISBN 3-11-002101-3 .
  • Reinhard Schönenberg, Joachim Neugebauer: Introduction to the geology of Europe . 4th edition. Verlag Rombach, Freiburg 1981, ISBN 3-7930-0914-9 , p. 167 ff .
  • Ralf Schuster et al: Explanatory notes to the map: Metamorphic structure of the Alps - Metamorphic evolution of the Eastern Alps . ( Online version; PDF file; 8.41 MB ; contains a section on the Lower Engadine window).

Coordinates: 46 ° 58 '15.2 "  N , 10 ° 23' 15.3"  E ; CH1903:  824,355  /  206418