Pohorje pluton

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The Pohorje pluton is a Miocene intrusive body of northern Slovenia .

geography

The Pohorje-Pluton, also Bacher-Pluton or Bachern-Pluton , is about 15 kilometers southwest of Maribor in the center of the Pohorje . The intrusion, elongated to the east-south-east, measures 27 kilometers along its longitudinal axis. Their broadside is between 4 and a maximum of 8 kilometers.

geology

The Pohorje pluton (in red) is located in the middle on the right edge of the map, at the transition to the Pannonian Plain (yellow-orange)

The Pohorje massif and the Kozjak upstream to the north form the crystalline massifs of the Eastern Alps that are furthest in the southeast . They are located on the western edge of the Miocene Pannonian Basin - a huge intramontane basin between the Carpathians , the Eastern Alps and the Dinarides . Both Massive consist of crystalline basement rocks and metamorphic Hüllserien of Austroalpine ceiling stack , which was carried out under high pressure to ultra-high pressure conditions tectogenesis the Eoalpine orogeny goes back 90 million years ago.

The intrusion took place in medium- grade paragneiss and almandine- bearing slate of the old crystalline shell series of the Middle Eastern Alps . Upon penetration, the host rock was metamorphically changed to andalusite-biotite-schist, the contact aureole can be traced around almost the entire pluton, recognizable by hornblende, hornfels , skarn and the occurrence of the minerals garnet and epidote.

The deepest tectonic unit in the Pohorje massif is made up of medium-grade, polymetamorphic rocks - the probably Precambrian Pohorje series - paragneiss, mica schist and amphibolite , in which marbles , quartzites , eclogites and serpentinites are sporadically inserted. At its structurally deepest section in the east of the Pohorje massif, the Pohorje series was affected by a Cretaceous ultra-high pressure metamorphosis. The exact age of the parent rocks could not yet be determined, as the series was completely influenced by the alpine orogenesis.

Above this, the uppermost tectonic unit is the low-grade Paleozoic ( Ordovician to Carboniferous ), the hanging wall of which is built up from the pyroclastic Magdalensberg Formation . Rare fossils made it possible to assign a Lower Devonian age to it. Discordant follow clastic, non-metamorphic Permotrias, scraps of Triassic dolomite, Gosaur remains and sediments of the Middle Miocene.

The original thrust orbit between the two tectonic nappe units - the Remschnig thrust - was then reactivated and / or deformed during the Upper Cretaceous and again during the Miocene when the Alpine orogen appeared and was exhumed. With the exception of the Middle Miocene, the Pohorje pluton intrudes all of the rocks listed above.

The Pohorje Massif is cut off to the west by the southeast- trending Labot Fault (Lavant Valley Fault), a dextral side shift . The Periadriatic Seam runs just 2 kilometers further south .

Petrology

Commemorative plaque made from cizlakite , a pyroxene hornblende diorite facies of the Pohorje pluton

The lenticular pluton has a calcareous affinity and is understood as either a laccolith or a tilted batholith . It consists mainly of gray, uniform-grain, medium to fine-grain granodiorite (with transitions to tonalite ), which can show localized transitions to a porphyry facies and also occurs as a subordinate quartz diorite . At the center of the intrusion are mafic enclaves. They are stretched out and, together with black streaks, give the rock a striped appearance. Cizlakite - a pyroxene hornblende diorite or quartz monzogabbro - is a huge mafic xenolite on the southern edge of the intrusion. It is probably an older Mafit / Ultramafit that was assimilated by the acidic magma.

White to light gray, 1 to 50 centimeters thick aplites and pegmatites , but also mafic (basaltic to andesitic) and Dacite dikes penetrate the intrusion and continue in the host rock. Smaller dacite bodies also appear on its surface . In its southeast section, the pluton also contains enclaves of the metamorphic host rock - a larger one sitting in the roof of the pluton at Veliki Vrh (with a contact courtyard) and a small, narrow one at the southeast end, which is elongated in the same direction and a right-shifting, also southeast-trending one Side shift follows.

The Pohorje pluton shows a flat parallel structure ( foliation ), which dips mainly to the south-southwest. It originated primarily magmatic but also in the ductile area due to progressive tectonic movements during the cooling process of the pluton. A lineation can also be seen with reference to the preferred orientation of the phyllosilicates and the relatively rare and hornblende based on a stretched, degraded and recrystallized quartz.

Mylonitic and cataclastic shear bands also developed locally . The roof area of ​​the pluton, especially in the northwest, was deformed brittle along the horizontal and is completely unusable as a building block due to the many disturbances.

mineralogy

Tonalite handpiece of the Pohorje pluton with pegmatite dike

The Pohorje pluton has the following minerals:

The quartz, which can grow up to 5 millimeters in size, is often completely dynamically recrystallized. In terms of quantity, the plagioclase outweighs the alkali feldspar by> 2: 1 and, as An 55, is quite anorthite-rich. It often has an oscillating zonal structure with An 52 in the core and An 26 at the edges. The alkali feldspar is an orthoclase that can be locally triclinized. The predominant dark part of the mixture is fawn to green, quite frequently occurring biotite, which can be chloritized. The hornblende is small and is either a magnesio hornblende or a Tschermakit or Ferrotschermakit . Muscovite , garnet (almandine) and, more rarely, beryl in aplite and pegmatite veins, allanite , apatite , epidote , rutile , titanite , zircon , zoisite , chlorite , carbonates and opaque minerals such as magnetite are worth mentioning as accessories .

The presence of myrmekite points to metasomatic processes , more precisely to a strong potassium metasomatosis of the original tonalite to granodiorite. Later studies by Trajanova (2013) were able to confirm these metasomatic processes, but limited them spatially to the area around the Remschnig thrust in the northwest of Pluton.

Cataclase can be recognized by plagioclases, which may be shattered and crushed at the edges, and whose lamellae are occasionally bent. The mosaic-like, undulant extinguishing quartz also point to a cataclase.

Chemical composition

Main elements

The following table is intended to illustrate the main chemical composition of the Pohorje magmatites:

Oxide
wt.%		 Diorite gabbro Cizlakit Quartz diorite Granodiorite Standard mineral
weight%		 Diorite gabbro Cizlakit Quartz diorite Granodiorite
SiO 2 52.40 53.70 55.10 65.60 Q 8.20 21, 20
TiO 2 0.43 0.46 0.45 0.39 C. 0.60
Al 2 O 3 6.20 7.41 10.40 17.20 Or 3.70 8.30 13.90
Fe 2 O 3 1.22 1.66 2.07 1.10 From 13.40 19.70 35.00
FeO 3.84 3.54 4.14 2.26 On 11.40 17.30 20.10
MnO 0.13 0.11 0.25 0.08 Tuesday 55.20 47.90
MgO 15.10 13.60 9.26 1.32 En 10.60 11.50 3.30
CaO 17.30 16.50 11.70 4.35 Fs 1.40 2.80 2.80
Na 2 O 1.17 1.57 2.25 4.10 Mt 2.40 3.10 1.60
K 2 O 0.44 0.62 0.54 2.33 Il 0.90 0.90 0.70
P 2 O 5 0.05 0.09 0.31 0.26 Ap 0.20 0.70 0.60
LOI 1.20 0.54 3.19 0.23

The bimodal rocks are sub-alkaline and at the same time of a calcareous character with a medium to high potassium content. These are granitoids of the I type. Their SiO 2 content varies between 52 and 66 percent by weight SiO 2 , so the igneous rocks are intermediate. The acidic granodiorites, but also the quartz diorites, are quartz-normative and therefore oversaturated with SiO 2 , the mafic terms are undersaturated with SiO 2 . The granodiorites are also corundum normative and therefore peraluminos . Quartz diorite and cizlakite are diopside normative and thus metaluminos.

Trace elements

Table with trace elements:

Trace element
ppm		 Diorite gabbro Cizlakit Quartz diorite Granodiorite
Cr 1648 1800 1100 60
Cs 0.89 1.10 1.80 3.20
Zr 54 62 82 223
Nb 7.0 5.0 4.0 16.0
Nd 20.6 23.0 23.9 39.8
Rb 16.0 22.0 26.0 86.0
Sr 279 470 480 910
Ba 286 620 150 1120
Th 6.48 7.70 0.50 25.0
Ta 0.26 0.52 0.45 1.57
Hf 2.02 1.90 1.30 5.40
La 22.9 23.4 8.45 58.8
Ce 45.0 47.1 28.1 111.0
Sm 4.26 4.85 6.33 6.50
Eu 1.03 1.08 1.39 1.41
Tb 0.52 0.517 0.785 0.710
Yb 1.90 1.26 2.08 2.29

Geochemically, the Pohorje pluton is quite rich in lithophilic elements ( LILE ) and shows very high contents of lanthanum and cerium . It is therefore regarded as a partial melt product of amphibolite and eclogite and can therefore not be classified under the periadriatic intrusiva - as was previously assumed. Nevertheless, there is an undeniable similarity to chemically comparable rocks of the Karawanken tonalite pluton , to the Re-di-Castello group of the Adamello pluton and to the Bergell pluton . This applies in particular to the trace elements hafnium , zirconium , yttrium , thorium and uranium , but also to most rare earths. The elementary ratios Ba / Sr, Ba / La, Nb / Th and Nb / U also show good agreement.

In the case of rare earths , the LREE are much more concentrated than the HREE . When applied, they show a very steep and consistent dip, which indicates the fractionation of hornblende. Only a weakly negative europium anomaly can be seen, which mostly occurs in the tonalites and indicates a moderate fractionation of feldspars. The HREE are very flat and low in concentration. This indicates fractionation of clinopyroxene and also reflects the pressure difference in the differentiation of the primary, mafic magma, which preferred the separation of amphibole over clinopyroxene , plagioclase and magnetite.

Isotope ratios

Isotope ratio Diorite gabbro Diorite Granodiorite 1 Granodiorite 2
87 Sr / 86 Sr 0.706659 ± 8 0.707594 ± 7 0.707062 ± 4 0.706993 ± 7
εSr 29.95 43.3 34.5 33.8
δ 18 O 6.7 7.0 7.7 7.9

The 87 Sr / 86 Sr ratios are relatively high and indicate crust contamination . The δ 18 O ratios vary from values ​​of the upper mantle (6.7 ‰) to crust values (7.9 ‰).

Petrogenesis

D18O-87Sr / 86Sr diagram showing the position of the Pohorje magmatites. Gabbro and diorite are on the AFC line, the granodiorites are crustally contaminated and scatter towards continental sediments.

As the main and trace elements suggest, the granodiorites and tonalites of the Pohorje pluton were formed by the fractional crystallization of a mafic magma that had also been contaminated by a considerable crustal component. The granodioritic / tonalitic plutonism was generally controlled by the subduction of oceanic crust prior to the Mesozoic , as well as by the metasomatosis of the overlying mantle wedge including the overlying continental crust. All analyzes confirm that the mafic predecessor agma was close to an olivintholeiitic composition. A slightly metasomatized garnet peridotite can be assumed as the melting source based on trace element modeling . The additional assimilation and fractional melting of crustal material (AFC processes) then resulted in crustal isotope signatures, which were reflected in the most acidic parts of the tonalite suite in particular.

Associated Dazite

At the northwest end of the Pohorje pluton, gray Dazitic dikes appear, followed outside the pluton by effusive dazites . The corridors run through steeply standing pluton and cladding rocks. In its microcrystalline matrix, quartz can be seen as a residual precipitate. Einsprenglinge are andesine with low and high temperature optics, biotite and occasionally green hornblende. The effusive dazites form chimneys, sticks and spring crests. Their basic mass is crypto to microcrystalline. Injections are corroded quartz, andesine only with high temperature optics, biotite (often chloritized) and occasionally hornblende. The surrounding paleozoic phyllites and limestones were changed to horn rocks and skarns in contact metamorphosis on Dacite stocks .

Pressure-temperature conditions

The following values ​​could be determined for the pressure-temperature conditions of the intrusion: a maximum value of 0.6 to 0.7 GPa corresponding to a depth of 16 to 19 kilometers should reflect the base of the magma chamber. Altherr and colleagues (1995) found a value of 0.68 GPa. These pressures correspond to temperatures of 760 to 820 ° C. The intrusion reached a final depth of 8 to 11 kilometers corresponding to a pressure of 0.3 to 0.4 GPa. The temperature at this level was around 750 to 770 ° C. It should be noted that the pluton in the east with 19 kilometers was probably deeper than in the west, where in return it penetrated very high and almost reached the weakly metamorphic Austroalpine at a depth of about 8 kilometers.

Age

The oldest radiometric age determination for the Pohorje pluton by Deleon (1969) was 19 ± 5 million years. A more recent study by Fodor and colleagues (2008) using the uranium-lead method on oscillating zonar zirconia (LA-ICPMS) was able to determine a much more accurate age of 18.64 ± 0.11 million years (early Miocene, Burdigalium ) In In the Eibiswald strata in the north of the Pluton, both tuff and pebbles from Dacite could be found. They have a Carpathian age (Upper Burdigalium, 17.3 to 16.5 million years) and thus provide a minimum age for the Dazites, for which the period 18 to 16 million years can be set.

The intrusion age of the Pohorje pluton is thus much younger than the other periadriatic intrusives, which are Oligocene . For example, the neighboring Karawanken pluton was dated to 32.4 ± 1.2 million years, which corresponds to the Rupelium . Overall, the ages of the Pohorje pluton show a good correlation with the magmatism in the Pannonian Basin in general and in the Styrian Basin in particular , which lasts from 19 to 15 million years .

The inherited zirconia cores have both Permian (290 to 270 million years) and Neoproterozoic (900 to 850 million years) ages and thus point to the melting and / or assimilation of crustal material with juvenile Neoproterozoic hafnium model ages. However, as hafnium isotope ratios (initial εHf) of the Miocene zirconia areas reveal, juvenile phanerozoic crust material must also have been involved or, alternatively, a Miocene mantle melt must be considered as a magma source.

The Cizlakite could be dated between 20.3 and 19.5 million years ago. It is therefore somewhat older than the actual Pluton. This is not surprising, since it represents a gabbroide inclusion in Pluton and is likely to arise from a mafic precursor magma.

tectonics

Ductile deformation

The Pohorje pluton had already been deformed in its igneous state, recognizable by an igneous foliation, which is mainly defined by biotite lamellae and horny needles, but is not always easy to separate from ductile foliation. Furthermore, two generations of gaits formed, the first of which consists of aplite and deformed Mafit and Dazite gaits. Some of the Dacite veins also show very nicely developed magmatic flow structures on a microscopic level. The first generation of dikes falls flat to moderately south to southwest and generally follows the foliation of the regional metamorphic rocks. However, the aplites are vertical with constant stroking. The second generation are undeformed Mafit and Dazite tunnels, which were created in fractures during an east-west stretching phase (see below). You therefore stand more or less upright and sweep from NNW to NNE.

After it was seated and crystallized, the Pohorje pluton and some of its dike rocks were ductile deformed in the solid state under green slate conditions (upper green slate facies). The medium-grade metamorphic rocks north and south of the pluton were also heated up again and then cooled down together with the pluton. This cooling and the further rise of the pluton and its host rocks were determined by actively advancing tectonics.

There are clear indications of the deformation in the solid state that occurred after magmatic crystallization. With well-developed foliation it can be seen that it often overprints the original igneous structure. Aligned biotites and horn apertures as well as elongated lenses of quartz feldspar aggregates also define a somewhat indistinct local stretching direction. In the south and south-west section of the pluton, the ductile foliation often follows the igneous, but is also NE and NNW-striking perpendicular to it with almost horizontal elongation lines that point in the east or west direction. The conditions in the north and northeast sections of Pluton are far more diffuse and difficult to interpret. The deformed Mafit and Dazite dikes largely follow the foliations in the south and south-west sections of the Pluton, but their elongation lines dip flat to moderately to the north-west.

Microtectonically , the deformation manifests itself in the solid state through complete recrystallization of quartz into elongated lenses. Primary biotite is sheared and recrystallized partially along the Foliationsebene with fine-grained, highly elongated edges (into so-called mica fish , English mica fish ). The feldspars show predominantly brittle behavior, but deformation twins, bent twins and incipient core-shell structures also point to a crystal-plastic behavior. Biotite and quartz tend to form incompetent, networked layers in heavily stressed rock sections - the typical eye gneiss structure is created. In less stressed areas, quartz partially recrystallizes, with indolent extinction and undersized grain formation being observed.

Brittle deformation

The cooling of the pluton had passed through the ductile area relatively quickly and it is estimated that after 3 million years it had already penetrated near the surface. This is confirmed by fissure trace ages of 17.7 to 15.6 million years. Its temperature was probably only between 300 and 250 ° C 17 million years ago.

After the pluton had reached the brittle area , it was subject to an east-west stretching in the Langhium (or Badenium ), which caused vertical thinning and north-south lateral shifts. This is related to the general, sideways extrusion of the Alps, which was effective in the Early and Middle Miocene in the Eastern Alps (the extrusion is to be understood as a combination of collapsing orogen with simultaneous continental evasive movement).

The end of this expansion phase is marked around 11.6 million years at the Serravallian / Tortonian (or Sarmatian / Pannonian ) border by northeast-southwest and east-west-directed compression, which below the Carpathian Mountains with a simultaneous change in the direction of subduction Relocation of the subducted foreland mass, as well as a back-arc opening in the Pannonian Basin.

The final stage in the deformation process in the last 7 million years from the Messinian (or Pontian ) was again dextral side shifts due to north-south to north-north-north-west-south-south-east directed compression, caused by transpression in the Dinarid-Alpid-Pannonian border area.

This threefolding in the brittle area can also be determined from faults using the method of Angelier (1984), which determines paleostress tensors on the basis of the measured harness stripes . The first, transtensional phase with east-west stretching is expressed in faults that only fall moderately in easterly directions, the movements of which shear off or obliquely in an easterly direction. The second phase was of a compressive nature with generally NE-SW to ONE-WSW-directed narrowing, characterized by steep conjugated lateral shifts. In the third and last phase, the narrowing turned to north-northeast (to northwest), again characterized by conjugate lateral shifts but also by upheavals. Faults in the first phase were partially reactivated.

Economic use

Work on blocks of the Pohorje pluton in the Cezlak quarry

Mineralization

In the first half of the 20th century, magnetite - hematite mineralization was discovered in the contact zone of the granodiorite , which was also mined. The iron ores are of iron sulfides, mainly pyrite accompanied subordinate also lead - zinc -Vererzungen as galena and sphalerite . In the eastern part of the Granodiorite, pyrite occurs only rarely. Other notable mineralizations in hedenbergite , epidote and garnet karnen (with andradite and grossular ) at Hudi Kot and Planina include azurite , bornite , chalcopyrite , chalcosine , limonite , malachite , marmatite , molybdenite and pyrrhotite . The skarns occur in contact with calcareous rocks.

As a stone

The Pohorje plutonite is the only magmatite used commercially in Slovenia and is considered to be a natural stone of high quality. It gives many larger cities in Slovenia a special touch. The granodiorite was mined in Josipdol near Ribnica na Pohorju and the variety Cizlakit since 1891 in the town of Cezlak near Oplotnica . The plutonite is pressure and bending resistant and is characterized by high density, low water absorption and low porosity. It is highly resistant to frost and salt. Because of these properties, it is widely used - as paving stone and, above all, as cladding panels in the interior and exterior of houses, shops, churches, public buildings, etc., including some listed buildings. The stone is also highly valued by sculptors for monuments and ornamental fountains.

See also

literature

  • Exner, Christof: The geological position of the magmatites of the periadriatic lineament . In: Negotiations of the Federal Geological Institute . Year 1976 issue 2, 1976, p. 3-64 .
  • László I. Fodor et al .: Miocene emplacement and rapid cooling of the Pohorje pluton at the Alpine-Pannonian-Dinaridic junction, Slovenia . In: Swiss Journal of Geosciences . Birkhäuser Verlag, Basel 2008, p. 1-17 , doi : 10.1007 / s00015-008-1286-9 .

Individual evidence

  1. ↑ Schmid, SM, Fügenschuh, B., Kissling, E. and Schuster, R .: Tectonic map and overall architecture of the Alpine orogen . In: Eclogae Geologicae Helvetia . tape 97 , 2004, p. 93-117 .
  2. ↑ Žnidarčič, M. and Mioč, P .: Geological map of the sheets Maribor and Leibnitz, L 33–56 and L 33–44, 1: 100 000 . Federal Geological Survey of Yugoslavia, Belgrade 1988.
  3. ↑ Hinterlechner-Ravnik, A .: Pohorski eklogit . In: Geologija . tape 25 , 1982, pp. 251-288 .
  4. ↑ Mioč, P .: Geology of the sheet Slovenj Gradec L 33-55 1: 100000 . Federal Geological Survey of Yugoslavia, Belgrade 1978, p. 74 .
  5. ↑ Janák, M., Uher, P., Ravna, EK, Kullerud, K. and Vrabec, M .: Chromiumrich kyanite, magnesiostaurolite and corundum in ultrahigh-pressure eclogites (examples from Pohorje Mountains, Slovenia and Tromsø Nappe, Norway) . In: European Journal of Mineralogy . tape 27 , 2015, p. 377–392 , doi : 10.1127 / ejm / 2015 / 0027-2436 .
  6. ↑ Kolar Jurkovšek, T. and Jurkovšek, B .: Lower Devonian Conodonts from the Pohorje Mountains (Eastern Alps, Slovenia) . In: Yearbook of the Federal Geological Institute . tape 139 , 1996, pp. 467-471 .
  7. ↑ Fodor, L., Jelen, B., Márton, E., Rifelj, H., Kraljić, M., Kevrić, R., Márton, P., Koroknai, B. and Báldi-Beke, M .: Miocene to Quaternary deformation, stratigraphy and paleogeography in Northeastern Slovenia and southwestern Hungary . In: Geologija . tape 45 , 2002, p. 103-114 .
  8. ↑ Zupančič, N .: Petrographic characteristics and classification of the Pohorje igneous rocks . In: RMZ - Materials and Geoenvironment . tape 41 , 1994, pp. 101-112 .
  9. ↑ Trajanova, M., Pécskay, Z. and Itaya, T .: K-Ar geochronology and petrography of the Miocene Pohorje Mountains batholith (Slovenia) . In: Geologica Carpathica . tape 59 , 2008, p. 247-260 .
  10. ↑ Trajanova, M .: Starost pohorskega magmatizma; nov pogled na nastanek pohorskega tektonskega bloka (Age of the Pohorje Mountains magmatism; new view on the origin of the Pohorje tectonic block), unpublished doctoral thesis . University of Ljubljana, Ljubljana, Slovenia 1994, p. 183 .
  11. ↑ Márton, E., Trajanova, M., Zupančič, N. and Jelen, B .: Formation, uplift and tectonic integration of a Periadriatic intrusive complex (Pohorje, Slovenia) as reflected in magnetic parameters and paleomagnetic directions . In: Geophysical Journal International . tape 167 , 2006, p. 1148-1159 .
  12. ↑ H. Kagami, P. Ulmer, W. Hansmann, W. Dietrich and RH Steiger: Nd-Sr isotopical and geochemical characteristics of the Southern Adamello (Northern Italy) intrusives: implication for crustal versus mantle origin . In: Journal of Geophysical Research . tape 96 , 1991, pp. 14331-14336 .
  13. ^ F. von Blanckenburg et al: Nd-, Sr-, O-isotopic and chemical evidence for a two-stage contamination history of mantle magma in the Central-Alpine Bergell intrusion . In: Contrib. Mineral. Petrol. tape 110 , 1992, pp. 33-45 .
  14. ↑ Altherr, R., Lugović, B., Meyer, HP and Majer, V .: Early Miocene post-collisional calc-alkaline magmatism along the easternmost segment of the Periadriatic fault system (Slovenia and Croatia) . In: Mineralogy and Petrology . tape 54 , 1995, pp. 225-247 .
  15. ↑ Deleon, G .: A Review of Absolute Age Determination on Granitic Rocks from Jugoslavia . In: Radovi Instituta za geolosko-rudarska istrazivanja i ispitivanja nuklearnih i drugih mineralnih sirovuna . tape 6 . Belgrade 1969.
  16. ↑ a b László I. Fodor et al .: Miocene emplacement and rapid cooling of the Pohorje pluton at the Alpine-Pannonian-Dinaridic junction, Slovenia . In: Swiss Journal of Geosciences . Birkhäuser Verlag, Basel 2008, p. 1-17 , doi : 10.1007 / s00015-008-1286-9 .
  17. ^ Frisch, W., Dunkl, I. and Kuhlemann, J .: Postcollisional orogen-parallel large-scale extension in the Eastern Alps . In: Tectonophysics . tape 327 , 2000, pp. 239-265 .
  18. ↑ Fodor, L., Csontos, L., Bada, G., Györfi, I. and Benkovics, L .: Tertiary tectonic evolution of the Pannonian basin system and neighboring orogens: a new synthesis of paleostress data. In: Durand, B., Jolivet, L., Horváth, F. and Séranne, M., The Mediterranean basins: tertiary extension within the Alpine Orogen (Eds.): Geological Society, London, special Publications . tape 156 , 1999, pp. 295-334 .
  19. ↑ Angelier, J .: Tectonic analysis of fault slip data sets . In: Journal of Geophysical Research . 89, B7, 1984, pp. 5835-5848 .