Geology and Tectonics of the Eastern Alps

59 Pages·2012·9.37 MB·English

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Abh. Geol. B.-A.
26e C. G. I. 34 p. 197—255 52 figures Wien 1. 5. 1980
International Geological Congress
26th Session
Excursion 035 A
Geology and Tectonics of the Eastern Alps
(Middle Sector)
by
ALEXANDER TOLLMANN
With contributions from A. FENNINGER, W. FRANK, B. PLÖCHINGER, S. PREY, J.-M. SCHRAMM & G. TICHY
Author's address: Geologisches Institut, Universität, Universitätsstraße 7, A-1010 Wien, Austria.
©Geol. Bundesanstalt, Wien; download unter www.geologie.ac.at
Contents 9th day: The Grauwackenzone and the Northern
Limestone Alps in Salzburg (B. PLÖCHIN-
Summary 198
GER, J.-M. SCHRAMM & G. TICHY) . 246
A) General introduction (A. TOLLMANN) . . .. 198
1. Literature 198
2. The geological position of the region visited Summary
within the European framework . . .. 198 The excursion into the middle sector of the Eastern Alps
3. The geological peculiarity of the Eastern Alps . 200 will demonstrate by selected examples along two cross-sec
4. The main structure of the Eastern Alps in the tions the stratigraphy, the different facies regions, meta
section visited 200 morphosis, nappe structure and microtectonics. The sequence
5. Paleogeography and orogenic cycles . . . 202 of nappes will be shown along the meridian of Salzburg and
6. Characteristics of the main units of the Eastern of Hallstatt. The Penninic nappe system appears as the
Alps in the region visited 204 deepest tectonic unit in the center of the Eastern Alps in
7. Remarks to the mineral deposits in the scope the region of the window of the Hohe Tauern. It is charac
of the excursion 209 terised by an eugeosynclinal facies and by a high degree of
B) Excursion description 210 metamorphosis. Above this lowermost unit follows the vast
1st day: Ultrahelvetikum and Flysch in Upper system of Austroalpine nappes ("Ostalpin"), devided into
Austria near Gmunden (S. PREY) . . 210 three distinct tectonic units: At the base the Lower
2nd day: The Hallstatt Zone and its framework Austroalpine nappe system, which is represented by the
near Hallstatt (A. TOLLMANN) . . . 214 Radstädter Tauern; the Middle Austroalpine
3rd day: Tectonics and facies of the Hallstatt system, which forms especially the large masses of Alt-
Zone in the eastern Salzkammergut kristallin in the central axial region of the Eastern Alps
beyond the Tauern Window only with a thin and uncomplete
(A. TOLLMANN) 219
4th day: The Lower Austroalpine of the central mesozoic cover under specific facies; the Upper Austro
Radstadt Tauern (A. TOLLMANN) . . 222 alpine nappe system, which comprises firstly the Northern
5th day: Lower Austroalpine unit in the southern Limestone Alps marked by a typical Tethys facies (aristo-
part of the Radstadt Tauern (A. TOLL- geosynclinal facies) rich in fossils, then the Grauwackenzone,
furthermore rests of this sheet in the Central Alps like the
MANN) 229
Gurktal nappe and a remainder near the root zone, the
6th day: Middle Austroalpine and Gurktal nappe
Drauzug in the Gailtal mountains. In its southernmost point
east of the Tauern Window (A. TOLL-
the excursion reaches the northern margin of the Carnic Alps,
MANN) 233
part of the Southern Alps. The northern rim of the
7th day: The late Paleozoic of the Nassfeld Area
Alps is shown in the Helvetic Zone with its series
in the Carnic Alps (A. FENNINGER) . . 238
under miogeosynclinal facies, overthrust by the Flysch
8th day: The Penninic System along the Groß-
nappe.
glockner road (W. FRANK) . . .. 241
A) General Introduction
By A. TOLLMANN
1. Literature
We can restrict the general introduction to this ex J. GEYSSANT & A. TOLLMANN: Alpes autrichiennes, C. r. Soc.
cursion, because you will receive a short "Einführung geol. France, 1966/11, p. 413—472, Paris 1966. — In Ger
in die Geologie Österreichs" on the occasion of this man: H. BÖGEL & K. SCHMIDT: Kleine Geologie der Ost
congress. Therefore you will find in the following pri alpen, 231 p., Thun (Ott-Verlag) 1976; W. DEL-NEGRO: Ab
riß der Geologie von Österreich, 138 p., Wien (Geol. Bundes
marily those special instructions, concerning the middle
anstalt) 1977; M. GWINNER: Geologie der Alpen, 477
sector of the Eastern Alps, visited by this excursion.
p., Stuttgart (Schweizerbart) 1971; A. TOLLMANN: Mono
In the following some newer books and papers concerning
graphie der Nördlichen Kalkalpen, vol. 1—3, Wien (Deuticke)
this matter are mentioned: In English: E. OXBURGH: The
1973, 1976; Geologie von Österreich, vol. 1: Die Zentral
Eastern Alps — a geological excursion guide, Proceed, geol.
alpen, 766 p., Wien (Deuticke) 1977.
Assoc, 79/1, p. 47—124, Colchester 1968. — In French:
2. The geological position of the region visited by the excursion within the European
framework
(Fig- 1)
The Eastern Alps represent a sector of the northern in the alpidic era indicate a general northward direction.
branch' of the young, alpidic Mediterranean mountain The main structures were built during Upper Creta
system. In this part of the Alps the tectonic movements ceous and Lower Tertiary. The orogenesis diminished
198
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| area visited by the excursion
| direction of movement
P R E C AM B R I AN
B A S E M EN
V A RI SC I D E 5
TAURIDE<iE
Fig. 1: The position of the Eastern Alps and the excursion route within the geological framework in Europe.
the width of the geosyncline from nearly 1000 km in Europe to the Pontides in northern Anatolia and
during the middle Mesozoic to approximate 150 km to the Elburs. The southern branch of this Mediterranean
today. system, mooving generally southwards, is comprised of
The northern branch of this young Eurasiatic moun the Rif, the Maghrebides within the Atlas, the Apen
tain system, built up of rests of the floor of the Meso nines, Southern Alps, Dinarides, Hellenides in Europe,
zoic Tethys ocean, leads from the Betic Cordillera in Taurides in the Turkey, and leads to the Himalayas.
Spain, from the Alps, Carpathians and the Balkans This mountain system arised from the wide Tethys
199
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ocean, which also contained the longish Kreios Plate the Carnic Alps and in the Altkristallin of the Middle
with its continental crust, and a lot of younger micro- Austroalpine system. This Variscic system is preserved
continents. The orogenesis was produced by the collision in a width of about 600 km maintaining a continuity
of the African and the Euroasiatic plates during the in the alpin foreland in middle Europe. In front of the
Cretaceous and the Tertiary. In the Eastern Alps a part Eastern Alps we find it in the form of the Bohemian
of the former, older mountain system, the Variscides, Massif with internal Variscic nappe structure, with
are preserved with its old tectonic structures, e. g., in a southeastern direction of movement.
3. The geological peculiarity of the Eastern Alps
The Eastern Alps are dominated by nappe structure. can be dated as pregosauic, that is equal to the Mediter
Six nappe systems are piled up in this chain. Each nappe ranean phase in the upper Turonian 90 million years
system in itself consists of individual nappes. The width ago. This data is in accordance with the radiometric
of the main nappe transport vary from some ten kilo age of the metamorphosis in the Austroalpine system
meters up to 165 km (Upper Austroalpine nappe sys ("Schneeberg crystallisation"). In this time the Penninic
tem). Already during the stage of geosyncline in the system of the Hohe Tauern was subducted beneath the
Mesozoic these units had individual facies. There are Austroalpine units. The younger main phase of trans
also differences in the distribution of the non-meta- port of the nappe systems is the Illyric-Pyreneen phase
morphic Paleozoic in the different nappe systems. Most at the end of the Eocene. During this time the central
of the nappes also contain crystalline rocks as remainders units of the Eastern Alps were transported above the
of a continental crust; only in the southern part of the marginal units. In this way vast parts of these marginal
Penninic nappe system are hints of a direct sedimen zones (Flysch Zone, Helvetic Zone) were covered and
tation of Mesozoic on oceanic crust. the sedimentation was finished in this region. A new
The considerable shortening of the crust in the foredeep formed. The Alps entered their Molasse stage:
Eastern Alps during the alpidic orogenesis produced Beginning with the Upper Eocene the debris from the
a crustal thickness of 50 km in comparison with 33 km Alps and the foreland accumulated in the Molasse Zone.
thickness of the crust of the Central European foreland. The younger phase of metamorphosis in the Eastern
Only in its eastern part the crust beneath the Alps thins Alps, dated in the Penninic system, occured in the
to 27 km, as below the Pannonic Basin in Hungary. Lower Tertiary and is perhaps in connection with the
This attenuation is a young effect in connection with second main thrust mentioned above at the end of the
the exaggeration of the Carpathians bend according to Eocene. In the lower part of the Penninic system in the
the principle of back arc basin forming. Hohe Tauern the metamorphosis then just attains the
The piling of the alpine nappes took place in various amphibolite facies.
phases. Shortening of the crust and subduction began After the reduction of the tangential pressure within
already in the younger part of the Lower Cretaceous: the upper Tertiary the orogenesis, characterized by
Austroalpine phase of the Barreme-Aptian, Austrian nappe building, is replaced by vertical isostatic move
phase of the Upper Albian-Cenomanian. During this ments. This late phase of mountain building is called
time the main central nappe systems began their "montigenesis", leading to the morphological forming
migration. The main nappe building in the Upper of mountains: big masses rise to considerable hights, on
Austroalpine system may be fixed by the Gosau for the other hand great basins are formed. In the Pliocene
mation, superposing in disconformity the limits of the the chain of high mountains is nearly complete and will
nappes in the Northern Limestone Alps. Therefore the be finished in the Pleistocene by the activity of the vast
thrusting of the nappes in this part of the Eastern Alps glaciation.
4. The main structure of the Eastern Alps in the section visited
(Fig. 2, 3)
In the middle sector of the Eastern Alps we find the c) Upper Austroalpine nappe system: Northern Lime
following main tectonic units, advancing from north to stone Alps (Mesozoic) and Grauwackenzone (Pa
south, from the frontal part of the mountain chain to leozoic)
the lower units of the Central Alps: d) Middle Austroalpine nappe system: Altkristallin
a) Helvetic Zone and Stangalm Mesozoic in centralalpine facies
marginal units
b) Flysch Zone e) Lower Austroalpine nappe system: Crystalline por-
200
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ft old crystalline ^jl}f Crystalline K Pennine of Rechnitx
Fig. 2: Tectonic sketch of the Eastern Alps (A. TOLLMANN, 1978) with the excursion route.
tion, Paleozoic and metamorphic Mesozoic in cen- Figures 2 and 3 show the arrangement of this nappe
tralalpine facies in the Radstadt Tauern pile.
f) Penninic Zone: Tauern Window with Crystalline The Penninic system appears as the lowermost
portion, Central Gneiss, Schieferhülle with Paleo unit in the large culmination in the center of the Eastern
zoic and Mesozoic parts. Alps, namely in the Tauern Window.
Flysch zone Grauwacken zone SURKTAL NAPPE
Helvetikum Northern Calcareous Alps M. and Lower Austroalpine Upper Austroalpine Drau unit
Traunstein Hohe Schrott Dachstein Stangalm Dobratsch
Molasse zone
X I
x x x x x x x x x x x xx
x x x x x x x x x x x x xx
L L L. L L
PENNINIC TAUERN WINDOW
D DACHSTEIN NAPPE
HA HALLSTATT ZONE 25 50
T TIR0L1KUM —I— =1
& BAJUVARIKUM
Fig. 3: Cross section in the middle sector of the Eastern Alps (A. TOLLMANN, 1976, fig. 9).
201
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The units of the Austroalpine system origi famous non-metamorphic Mesozoic series, rich in for
nate from the region south of the Tauern and were mations and fossils, e. g., the Hallstatt Limestone with
thrust on and above the Tauern Pennine towards the the great number of ammonites. The internal nappe
north. The Lower Middle Austroalpine unit rested in structure of the Limestone Alps offers eminent compli
the Central Alps, covers the Pennine and shows speci cations. The Palaeozoic basement of the Limestone Alps
fic, slight metamorphic Mesozoic series in "central- appears in the Grauwackenzone, built up of low meta
alpine" facies, poor in fossils. The Drauzug southern- morphic series of fossiliferous formations. As an impor
ward of the Tauern Window and the Northern Lime tant remainder in the same position as the Grauwacken
stone Alps thrust far above the Hohe Tauern, belong to zone we see the Paleozoic mass of the Gurktal nappe
the Upper Austroalpine unit. These two comprise a within the central zone of the Eastern Alps.
5. Paleogeography and orogenic cycles
Figure 4 shows the pattern of the main facies regions series of marly and detritic sediments, also with graded
during the time of geosyncline prior to the orogenesis. bedding are produced, alternating with submarine basic
a) A specific zone developed in the cental part of the effusiva with pillow structure — today metamorphosi-
Tethys during the Upper Permian in the Northern zed to blueschists, greenschists and eclogites. Masses of
Limestone Alps, characterized by the Haselgebirge, rich breccias in the Penninic and Lower Austroalpine area
in salt, gypsum and anhydrite. demonstrate the high mobility of the crust.
b) During Triassic time distinct differences existed d) At the end of the Lower Cretaceous the
between the facies zones of the Alps, generally arran geosyncline was transformed to the orogen. During the
ged in longitudinal direction: The Helvetic zone still Middle Cretaceous the subduction started. The
did not exist; the Penninic realm shows miogeosyncli- sedimentation in the present lowermost tectonic units
nal facies with variegated schists and sandstones in the in the Central Alps ended, because they were covered
Upper Triassic; in the Austroalpine region the Triassic by thrusts of higher nappe sheets. In the uppermost
contains sediments of a carbonate plattform type, tectonic unit, the Upper Austroalpine system, the sedi
whereby the thickness increases southward up to some mentation during the Cretaceous became very incom
kilometers. The northern part of this region include the plete. It ends early in the Drauzug and in the southern
"centralalpine" facies, the southern one the "nord- part of the Limestone Alps, continuing only in the nor
alpine" facies. To the latter belong the Northern Lime thern part of the latter. After the revolution by the
stone Alps, which show the Hauptdolomit facies (with nappe formation in the course of the Mediterranean pre-
the Norian Hauptdolomit) in the north, and the Dach gosauic phase marine sediments were deposited in the
steinkalk facies (with the Norian-Rhaetian Dachstein Limestone Alps only in some local "Gosau" basins
limestone) in the south. In the last-mentioned region during Senonian and Lower Tertiary. In the Eocene the
the Hallstatt facies (with thin red Hallstatt limestone in sedimentation terminates definitely in the Northern Li
the Middle and Upper Triassic) is intercalated in some mestone Alps.
narrow channels. e) The coherent sedimentation during the Ter
c) While the continental crust of the geosyncline tiary at first was restricted to the Flysch Zone and
attenuated in the Triassic by fracturation and the first Helvetic Zone in the north of the Alps, joining the
vulcanites appeared, it began to burst during the Jur Cretaceous series of these units. The Helvetic realm
assic time. In the northern and southern part of the contains the sediments of the shallow shelf of the Bohe
Penninic realm an ocean floor built up the basement mian Massif, rich in macro- and microfossils, divided
for the following sedimentation (Glockner nappe in the into a northern subzone, rich in limestone (correspon
southern Pennine, perhaps of the Flysch Zone in the ding to the Helvetic Zone of Switzerland) and a sou
northern Pennine). As a consequence of attenuation thern one, rich in variegated marls (named Ultrahel-
and the opening of the continental crust, the floor of vetic Zone). Adjoining to these marginal zones in the
the Tethys ocean subsided in accordance with the lows south, we find the Flysch belt, a long and deep trough,
of isostasy. Therefore in the Jurassic sediments like marl, produced by the beginning subduction in the region of
clay, chert and pelagic limestone dominated, accompa northern Pennine. The series of this trough are parti
nied by red nodular limestones. Carbonate platform ally preserved in the Rhenodanubian Flysch Zone. Here
sediments like reef limestone (Plassenkalk) only reappear
in the Northern Limestone Alps toward the end of the
Jurassic.
Fig. 4: Paleogeographic sketch of the main facies zones of the
In the eugeosynclinal Penninic realm of the Hohe Eastern Alps during geosynclinale stage in the Triassic and
Tauern during the Jurassic and Lower Cretaceous big Jurassic (A. TOLLMANN, 1978, fig. 2).
202
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+• t +• +
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RECENT: Deep Mountain roots
BM Bohemian Massif
rIO Molasse
HE He.lve.Kcum
Fy Flysch Zone
NP North Pennine
MIOCENE: tfolasse stage
UP Ultrapienidic Rise
MO HE UA _-
MP Middle Pennine
5P South Pennine
LA Lower Austroalpine
MA Middle Austroalpine
LATE EOCENE: Subductionof the Northern zones
UA Upper Austroalpine
MOL
5A Southalpine
PA Penadriatic Suture
N U.CRETACEOUS'. Nappe Formation mithin the Austroalpine
HE Fy UA
M. CRETACEOUS: Begin of the Penninic Subduction
LA MA UA SA
1
^ IH^.
U.JURASSIC/L.CRETACEOUS: Oceanfloor spreading
(NP) MP SP
UTRIASSIc: Extension of the Crust
VORLAND | NORTHERN ALPS SOUTHE.RN ALPS
^JZU^MSZ 233
E /UP MP \SP / LA/'^MAT
Fig. 5: Model of the genesis of the Eastern Alps shown by the sequence of stages from geosyncline to orogene in schematic
sections (A. TOLLMANN, 1978, fig. 3).
we find a typical flysch sediment with all characteristics The change from the Helvetic stage to the Molasse
of this type of sediment as graded bedding, flute casts, stage mentioned above occured within the Upper Eocene.
specific ichnofacies etc. Furthermore this trough with The exogeosyncline of the Molasse received marine se
his typical "orogenic" sediments, formed a new element diments till the Karpatian at the end of Lower Mio
in the Eastern Alps, established oblique to the older zo cene.
nes, running from the Northern Penninic region in the Figure 5 shows the tectonic development of the Eastern
west to the Helvetic region in the east, so that the se Alps.
dimentation took place on different basement.
6. Characteristics of the main units of the Eastern Alps in the region visited by the excursion
In the following the tectonic units mentioned above tonic positions to those in lower ones — except for the
will be characterized by stratigraphic range, tectonic marginal units in the north.
style and degree of metamorphosis. Figure 6 gives an a) The Helvetic unit contains a Mesozoic series
orientation about the stratigraphic sequences of all units, from the Liassic Gresten beds to the pelagic limestones
visited by the excursion — therefore, a description in and marls of the Cretaceous and the marly Lower
the text is unnecessary. Tertiary. The thickness of these series is moderate. The
The description below treats the units in the order influence of the German foreland in litho- and biofacies
of north to south, that is, from the units in higher tec is evident. The younger part of the sequence, comprising
204
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Cretaceous and Tertiary, shows a distinct difference be nel can be seen in the Mandlingzug near Radstadt; the
tween a northern subfacies rich in limestones and a southern channel joins at the southern rim of the Dach
southern one rich in marls. The contrast between the stein massif — tectonical outliers of this southern chan
abundance of pelagic foraminifera in the Cretaceous nel are preserved near Mitterndorf in the Styrian Salz-
and Tertiary formations in the Helvetic realm, and the kammergut. Mount Plassen near Hallstatt also seems to
poverty of those in the neighbouring and overthrust derive from this channel.
Flysch nappe (which contains especially arenaceous fora
This middle part of the Northern Limestone Alps was
minifera) is striking.
divided by the orogenesis during the Mediterranean
The Helvetic Zone is almost totally thrust by the phase in Turonian time into the following nappes, piled
flysch nappe. It appears only with frontal parts and from bottom (north) to top (south): Lunz nappe with
by slit-like tectonic windows on the surface. It was the Langbath Mass, the Staufen-Höllengebirge nappe,
also found in boreholes beneath the Flysch. the Totengebirge nappe. These three units show mainly
b) Flysch Zone: This unit is totally stripped Hauptdolomit facies (only the latter passes to the Dach
from its basement, which was built by the older Meso- steinkalk facies), followed by the Zlambach Mass (Hall-
zoic beds of the northern Pennine and the southern Hel statt facies), the Warscheneck nappe, the Mandling Mass,
vetic Zones. The series of the Flysch unit ranges from the important Dachstein nappe and finally isolated out
Albian to Eocene. The Upper Cretaceous part presents liers of the southernmost Hallstatt unit, that is, the
in the best way the particularities of flysch facies. The Mitterndorf nappe. The contrast in facies and thickness
participation of Tertiary formations diminishes toward of the latter units is striking.
the west and increases toward the Carpathians in the
The great rock-masses of the Limestone Alps did not
east. The flysch sediments were deposited in the deep
suffer a metamorphosis. However in the southern third
sea, dominating below the CCD. The paleocurrents
of the mountain one can see an anchimetamorphic trans
were directed westward.
formation. Finally, in the basal beds of the southern
In this sector the Flysch Zone forms only one nappe, margin one can find low graded greenschist metamor
strongly folded internally. This sheet is divided into phosis.
three nappes only far in the east, in the Vienna Forest.
d) Grauwackenzone. It forms the strati-
The flysch, overthrusting the Helvetic Zone, is itself
graphic basement of the Limestone Alps and therefore
overthrust by the Northern Limestone Alps. One can
occurs along the southern margin of these mountains
find flysch windows in two thirds of the Limestone Alps.
bordering the Altkristallin of the Central Alps. This
The beds of flysch rest in an un-metamorphic state.
zone comprises a sequence from the Ordovician to the
c) Northern Limestone Alps (Calcareous Upper Carboniferous. In the Lower Palaeozoic slates
Alps): The sequence of this unit passes from Permian dominate. Vulcanites of basic or acid character and car
up to Eocene. The morphological features are deter bonates also participate in the composition of the Grau
mined by thick carbonate masses of Triassic age, which wackenzone. Coarse detritic Upper Carboniferous is re
form large massifs of dolomite and limestone, while the duced in this middle part. Variscan and Alpine tectonics
Jurassic marls and slates are insignificant for rock face affected this zone. During both orogenesis the meta-
formation. Figures 4 and 6 show the Triassic facies zo morphism attained only the greenschist facies.
nes of the Limestone Alps. Some remarks on this compli In the Central Alps, the excursion arrives at the
cated matter: the Hauptdolomit facies includes in this western border of the Gurktal nappe, which re
region in the Middle Triassic Ladinian Wetterstein lime presents a part of the Upper Austroalpine. It con
stone, in the Upper Triassic Hauptdolomit and the marly sists of a very thick mass of slates of Ordovician and
and calcareous, fossiliferous Rhaetic Kössen beds. The Devonian age (Eisenhut slates), few carbonates and a
Dachsteinkalk facies, adjoining to the south, comprises thick Upper Carboniferous mass of sandstones and con
vice versa the (Ramsau-)dolomite in the Middle Trias glomerates. This nappe with a width of 60 km is thrust
sic and thick limestone (Dachstein limestone) in the far in a northern direction, in consequence of the west-
Upper Triassic. The reefzone of this carbonate platform east orientation of its fold axis, combined with the un
in the Upper Triassic appear in the southern region of derlying Stangalm Mesozoic along its western rim.
Dachsteinkalk facies, divided into many individual reefs,
e) Middle Austroalpine: The vast and thick
while the northern part is formed by thick bedded Dach
Altkristallin of the Central Alps outside the Tauern
stein limestone of lagoon type. A detailed reconstruc
Window, which is touched during the excursion in the
tion of the original position of the channels with Hall-
Schladming Tauern near Radstadt, along the Lieser
statt limestone in between the platform sediments is still
valley in Carinthia and between Kreuzeck and the
to be made.
Schober mountain NE of Lienz, does not form the nor
Now one supposes three channels with Hallstatt facies mal basement of the Paleozoic mentioned above. It
within the Dachsteinkalk area: The northern one in the represents — as decided only twenty years ago — an
region Ischl—Grundlsee is characterized by a facies rich independent tectonic unit, a typical basement nappe
in marls in the Upper Triassic; rests of the middle chan with only few remnants of its own Mesozoic cover in
205
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ZONE MOLASSE ZDNE HELVETIKUM ULTRAHELVET. FLY5CH ZONE PENNINE ZONE LOWER AUSTRO-A. MIDDLE AUSTRO-A
.FACIES Germanic facias Miogeosyndinale facies Eugeosynclinala facies
Centralalpine facies
within
Penninic facies
TIME
the basement Flqsch facies Hochsteg Brennkgl Glockner Hochfeind Pleisling Stangalm
part.beloui CCD fades (rise) facies facies facies facies (GurktaL Alps')
M.-U. MIOCENE
NE06ENE Fresh-water series
L.MIOCENE
-U. EOCENE ti.fcöc. stockleHen
PALEOGENE Molassc marine MLP.AE.ELOOECCQC.. AM. dLi1dihthhiol-ol,2Rlh-o,a£temrzrz-nb .bclsadtds. s EDVCaEriMegEa-PteAdL EmDaCrtE NE LPALEQ6ENE-
marls, sandst. Numrnulitic limest. -U.CAMPANIAN:
UPPER CRET. UC.ECMGNAarMOerleFMsnA,As NasNInaAldAnNsdN-tlso.:Ttt noUenRseO N. SrgUEugRmNaOu:t eNNdI:A RSmNepaidoGrmttlrseen dur lJslvi,mlasreti,es -t. SEVsNpaoOriteNtgeIAadt Nem-dA aLarBnlsIdA N UUZeppSsmpphoeeaeftrrln mvestasmoan sneetrd qvgs.ae ts lon hsneaeegler aisete sd
ALSIEN: Black marls Reiselsberq sandst. Kaserer series 5chmarz=
LOWER CRET. UL..NNEEQDCCODMM.-..-B.AIapctky cmhaursls GU-aNueltp cqouma.r tzHitues ch Bshüinsdtse n seecrki-es:
Massive limestone Aptychus limestones, Hochsteg II qbureacrctzia. ,
MALM and dolomite Vulcanites limestone-, n .(Aptychus" Limest.
p.p.oolitic dolomite "Aptych'lst.,
Glauconitic sandstone Ruhpolding chert Chert mit-h manganese Chert with mangan.
DOGGER WNaieduhhoatuesn baendds Phyilite Tküorkgeenl- - VCliiomrlineeosttit d. . Scilaiclec-osuhsa les
LIAS G(r"eLsitmeens bt.,e dmsa rls, Hochsteg l! ssbelraerctieecissa,: s Bcslaalaclckte =s Sandy shales
•rkose tcoal) quartzite Limestone tCrinoides
U.Rhaetian limestone Calcphyllites
RHAETIAN
Kassen beds
Keuper:
Variegated Platfenkalk
N0R1AN Hauptdolomit
shales and Hauptdolomit
sandstone
Camion dolomite Dolomite, breccia,
CARNIAN Locally 3 E Breccias, shales Cidans limestone *
remnants Locally Partnach dolomite Black shales
of remnants Wetterstein Tuffs
LADINIAN Pseedrmimotern'iatss sic oafn alog. dolomite LddeoHloemrsittee in
Permo = TrDchites dolomite Dolomite
AN15IAN (analogous Marble triassic Dot, streaky limest, Banded
to RaLuuahc-ke sedim. SRaanudhieuda clkiem estone Raliumheiusatocnkee
the other
Alpine f?Dt shales Alpine Rötshaies
5KYTH1AN Penninic Lontschfeid 5emmenng
series) quartzite quartzite
ZECH5TEIN Alpine Verrucano-. Alpine Verrucono:
5enzJt-and Quartzite,
ROTLIEGEND Phengite schists Quartzkera«
tophyre
WESTFALIAN:
SILE5IAN sandstone,conglo:
merate, schists
DINANTIAN
DEVONIAN
SILURIAN
ORDOVICIAN
CAMBRIAN
BASEMENT Bohemian Buch-monument NUolrttrhapheenlnveintiicc and Central gneiss III! Tmenq Liesertal
Crystalline granite socle Crystalline. Crystalline
Fig. 6: Stratigraphical sequences of the main units of the Eastern Alps in its middle sector.
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