Karawanken granite pluton

The Karawanken Granite Pluton is a Central Triassic intrusion in the Northern Karawanken .

geography

The Karawanken granite pluton, sometimes called Eisenkappel Granite or just as Krawanken Granite referred ( English Northern Karavanke Granite Belt or abbreviated NKGB ), consists of a 43.7 km long (of which 35.3 km in Slovenia and 8.4 km on Austrian territory) and mostly just under a kilometer wide granitoid lamella (maximum width 2 kilometers in Slovenia, 0.9 kilometers in Austria, minimum width 270 meters in Austria). It begins southwest of Eisenkappel directly at the Periadriatic Seam, passes almost a kilometer south of Eisenkappel in an alpine, east-west direction and then continues in the east in Slovenia, runs immediately south of Črna na Koroškem and Šentvid , and then north of Zavodnje (near Plešivica ) to end and disappear under sediments of the Pannonian basin . In Slovenia, the minimum width of the intrusion can even be reduced to zero in places due to right-shifting, south-east trending lateral shifts.

geology

The Karawanken granite pluton is the easternmost Central Triassic intrusion of the Alps. At a distance of about 2, at most 3 kilometers, it runs more or less parallel to the Periadriatic Seam , which is bordered on its northern edge by the Oligocene Karawanken tonalitic pluton . Between the two granitoid lamellae lies amphibolite facial , Austroalpine old crystalline (predominantly paragneiss , orthogneiss and phyllonite ). On its north side, the pluton pushes over the very low-metamorphic Variscan Eisenkappler Diabaszug (green slate facies, with a metamorphic age of around 300 million years), which was metamorphically changed to cordierite knot slate, as well as Triassic dolomites . The granite pluton has changed its host rocks on both the north and south side with contact metamorphism , but the two contact zones were later tectonized; the north contact is nowhere directly accessible and only documented by reading stones.

The elongated, narrow granite pluton is a tectonically transported and, as a rigid body, mylonitically deformed, thin, steep lamella. Together with the Karawanken tonalite pluton, it follows an east-west trending crustal weak zone in which tectonic and / or magmatic movements / activities took place from the early Paleozoic to the Quaternary (lithospheric flexure). From the Cenozoic era, the movements focused along the transpressive right-shifting periadriatic suture. The Karawanken tonalite pluton was therefore symmetrically deformed while it was being seated and ductile after cooling. In contrast, the Karawanken granite pluton owes its "ribbon-like", chopped-up appearance in the map to a purely brittle alpine deformation along the discrete lateral shifts mentioned above.

Pressure and temperature conditions

The intrusion into the host rock was very shallow, the depth was probably between 5 and a maximum of 8 to 9 kilometers. This corresponds to a pressure of ≤ 0.35 GPa , recognizable by the appearance of parageneses with andalusite and cordierite in the contact metamorphic altered neighboring rocks. This is also indicated by the composition of the hornblende edges (aluminum content barometry), which show around 0.3 GPa. The zirconium geothermometry reveals temperatures of 675 to 760 ° C (in granites), 794 to 801 ° C in granodiorites and possibly up to 838 ° C based on hornblende values ​​in monzonite. For gabbro the result was 1000 ± 20 ° C at a pressure of 0.38 to 0.47 GPa, which was thus much hotter and also deeper.

Petrology

TAS diagram with the compositions of the Karawanken granite pluton. The blue arrow shows the fractionation of the mafic differentiates, the yellow arrow that of the acidic rocks.

The very heterogeneous Karawanken granite pluton consists essentially of granite (better syenogranite) and diorite , as well as subordinate granodiorite (better syenite ), monzonite , monzodiorite, monzogabbro and olivingabbro . Diorite and gabbro take up about 30 percent by volume. Aplite and pegmatite are rarer differentiates . Mafic, comagmatic corridors also occur, which are occasionally penetrated by aplites. The main components of granite and diorite alternate in long lasting strokes and can penetrate one another. The internal rock boundaries are mostly steep to vertical. The strike directions are north-east, east-north-east and east-south-east, the latter direction predominates in the tectonically more stretched eastern part.

The porphyry granodiorite (syenite porphyry), well known for its beautiful Rapakiwi feldspars, usually lies between granite and diorite, but can also cross both with short corridors.

The gabbro appears as meter-sized inclusions in the diorite - but its inclusions in the granite are only in the decimeter and centimeter range. The mafic inclusions are rounded and indented, smaller inclusions are medium to fine-grained and show sharp, sometimes jagged, sawtooth-like contacts compared to the granite, which indicate their origin as deterred mafic magma cushions. These conditions are also present in other plutons and are seen as signs of spatial mixing of mafic with acidic magma.

Magmatic breccias with sharp-edged fragments of ultramafic rocks can be found in the porphyry granodiorite . They consist of 60 percent by volume of olivine, 30 percent by volume of amphibolitized clinopyroxene, brown amphibole and phlogopite , 5 percent by volume of calcium-rich feldspar and 5 percent by volume of magnetite , ilmenite and pyrite . These are undoubtedly mantle rocks that crystallized in the lower crust or in the upper mantle.

In the vicinity of the enclaves, the alkali feldspar megacrystals of the host granite are often encased in plagioclase. In addition, Ocelli structures are found in some of the intermediate rocks . It can also be observed that intrusive breccias have brought alaclifeldspar megacrystals from the acidic into the mafic magma. All of these three indications also indicate that an exchange between the two types of magma has taken place.

The rocks of the granite range are usually massive and generally show neither foliation , regional metamorphosis , nor hydrothermal changes. Only in local fault zones in the ductile area can post-crystalline foliation, diaphthoresis (retromorphism), mylonitization and even ultramylonite formation be observed, then in the brittle area fault areas with harnesses and finally hydrothermal recrystallization.

Petrography

Biotite granite (or syenogranite)

The massive granite occurs as uneven, medium to coarse-grained biotite granite, which has a trachytic structure . Its minerals are the two-generation minerals alkali feldspar , quartz and plagioclase , as well as biotite , hornblende and ilmenite with edges made of sphene , zircon and apatite . Monazite can occur in biotite , recognizable by radioactive reaction zones. Secondary formations are allanite , chlorite (according to biotite and hornblende), epidote , clinozoisite and sericite in the feldspars. The main component is first-generation alkali feldspar, which is pink, poikilitic, 20 to 30 millimeters in size, idiomorphic microcline or perthite / microperthite. It contains inclusions of plagioclase, quartz and biotite. The second generation is fine-grain microclinic. First generation quartz crystals are rounded and form inclusions in alkali feldspars. Second generation quartz crystals are fine-grained, form interstices or fill cracks. Plagioclase appears as cloudy, antiperthitic crystals with a wavy zonal structure. Its cores are often made up of oligoclase , which merges into albite at the edges . A special feature are the growing thin edges of myrmecite . The idiomorphic plagioclase of the first generation contains numerous micro-inclusions of an indeterminable nature, which document growth disorders. The second generation is less contaminated and grows up the first generation while maintaining the optical axes. The crystal clear quartz has a grain size of 10 millimeters. The idiomorphic biotite, only a few millimeters in size, consisting of 60 to 80% annite , forms random, lamellar, feldspar-shy aggregates. The edges of the idiomorphic hornblende are decomposed by late formations, mostly quartz. Hornblende usually breaks down into chlorite.

Granodiorite (or syenite)

The granodiorite is amphibole leader and what microstructures and mineral composition is concerned, very similar to the biotite granite. It also contains plagioclase, alkali feldspar and quartz with small additions of idiomorphic green hornblende. A special variety is the porphyry Rapakiwi granodiorite , which contains rapakiwi feldspar ovaries up to 30 millimeters in size, plus plagioclase strips and rounded quartz crystals. The medium to fine-grained base consists of microcline, oligoclase, quartz, brown biotite and green, 5 to 12 millimeter long hornblende . Accessories are apatite needles, ilmenite, sphene and zircon. Secondary formations are chlorite, epidote and carbonate . Orthite and garnet and possibly monazite are very rare . In the core of the Rapakiwi feldspar there is a rounded microcline perthite, which is encased in a coat mainly made of oligoclase (An ₁₉ ). In the mantle there are also small, calcium-rich, zoned plagioclase (core at ₄₀ and edge at ₂₁ ), graphic quartz and skeletal hornblende. The border between the microcline perthite and the mantle is formed by a thin shell of dendritic plagioclase and occasional small grains of quartz. The granodiorite also contains myrmecite, which penetrates from the oligoclase shell of the rapakiwiblasts into the surrounding microclines.

Diorite

The structure of the massive, medium and coarse-grained variety of diorites is usually serial (with constant grain size variability), but can also become porphyry due to the presence of plagioclase and hornblende phenocrystals. The minerals are composed as follows: plagioclase, hornblende , diopside , red-brown biotite only a few millimeters in size, interstitial quartz and microcline. Ilmenite, up to 2 millimeters long sphene, apatite, zircon, opaque minerals and secondary chlorite function as accessories . Plagioclase reaches a grain size of 5 millimeters and occurs both interstitially and idiomorphically. The interstitial plagioclase consists of An _8-23 , the idiomorphic plagioclase is zoned with An ₇₅ in the core and An ₅₂ at the edge. The hornblende, which can be up to 20 millimeters long, appears as a brown and green hornblende. The brown hornblende contains tiny grains of ilmenite and is framed by green hornblende. The green hornblende can also occur in isolation or displace clinopyroxene (diopside) in fine-grained diorites or dioritic enclaves. The microcline is usually interstitial but can sometimes grow up as an antirapakiwi plagioclase.

Gabbro

The massive gabbros, probably the best preserved in Austria, are uneven, fine to medium-grain rocks. They are made up of the minerals plagioclase, clinopyroxene, hornblende, biotite and quartz. Zircon, ilmenite, sphene and apatite needles up to 4 millimeters long can be used as accessories. Epidote, chlorite, and carbonate are secondary formations. For larger inclusions, up to 5 millimeters in size appears olivine (Fo _87-92 ). The predominant plagioclase up to 8 millimeters in size shows a zonal structure with An ₇₄ in the core and An ₆₅ on the edge. Its edge is also overgrown by oligoclase (An ₁₉ ). Xenomorphic plagioclase grains can be tectonically stressed and show deformed twin lamellae. Clinopyroxene, which can grow up to 3 millimeters in size, is diopsy (Wo ₄₅ En ₃₆ Fs ₁₉ ) and has a magnesium number of 0.65. It can tend to grain disintegration and Uralitization . The amphibole is brown to deep black hornblende up to 25 millimeters in size, the core of which is enriched with small ilmenite grains and sometimes also contains remains of clinopyroxene (hornblende can replace pyroxene). The red-brown, several millimeters large biotite forms interstitial plates with a magnesium number of 0.48. The gabbros occur as a fine-grained, isotropic variety or as a cumulate. They can lead to mafic and ultramafic inclusions.

Monzonite

The porphyry, fine-grained monzonites have phenocrystals made of microcline and plagioclase. The poikilitic microcline, which can grow up to 20 millimeters in size, is perthitic. The plagioclase forms idiomorphic, zoned crystals with a core of An ₃₁ and an edge of An ₂₀ . Contacts with microclinics are often covered with a myrmec border. The microcline, for its part, is occasionally coated with plagioclase. Quartz occurs in two generations. The first generation forms round grains and is surrounded by hornblende and biotite, sometimes accompanied by pyroxene and plagioclase. It is therefore a quartz ocelli. The second generation is fine-grained and corrodes phenocrystals of the first generation, cracks and veins in the plagioclase are filled. The dark brown biotite has a magnesium number of 0.28. It usually occurs interstitially and often forms inclusions in the relatively rare hornblende with a magnesium number of 0.35 or can also completely replace hornblende. Zircon and apatite needles are quite common, and muscovite and opaque minerals are also accessories. A characteristic accessory mineral, however, is dark red, idiomorphic allanite , which can reach a size of 2 millimeters. Secondary epidotes and carbonates can appear. Hornblende and biotite are quite often converted to chlorite .

Chemical composition

Main elements

The following table is intended to illustrate the main chemical composition of the Karawanken granite pluton:

Oxide wt.%	Ultramafic inclusion	Gabbro inclusion	Diorite	Monzonite	Syenite	Granodiorite	Granodiorite porphyry	granite	Syenogranite
SiO 2	43.70	50.78	55.53	61.77	65.77	68.78	68.80	73.89	75.16
TiO 2	1.79	2.02	1.67	0.44	0.36	0.40	0.42	0.22	0.13
Al 2 O 3	10.30	16.03	17.53	18.35	14.17	15.07	14.72	13.88	12.51
Fe 2 O 3		2.45	2.16	1.53		0.79		0.23
FeO	13.74 (dead)	6.00	5.44	2.52	2.17 (dead)	1.97	2.65 (dead)	0.71	1.15 (dead)
MnO	0.18	0.17	0.15	0.12	0.05	0.03	0.07	0.02	0.03
MgO	17.80	5.33	2.33	0.72	0.67	0.78	0.60	0.17	0.22
CaO	6.28	7.50	4.87	2.62	3.19	1.77	1.57	1.06	0.35
Na 2 O	2.17	4.34	4.55	4.80	4.83	4.42	4.63	3.70	3.93
K 2 O	1.19	1.21	3.34	5.64	5.42	4.05	4.66	5.15	4.57
P 2 O 5	0.30	0.50	0.61	0.19	0.17	0.22	0.16	0.14	0.04
LOI	0.85	2.35	1.51	0.2	2.78	1.2	0.72	0.83	0.51

The igneous rocks form an alkaline differentiation series with a calcareous to shoshonite character. K ₂ O and Na ₂ O are therefore very highly concentrated, especially in monzonite. Since K ₂ O is often more concentrated than Na ₂ O (especially in the acidic members), there is a potassic series. The SiO ₂ content fluctuates between 50 and 74 percent by weight, so the rocks are intermediate to acidic. The mafic gabbros and diorites are undersaturated on SiO ₂ , whereas all other links are oversaturated on SiO ₂ , indicated by normative quartz . The granodiorites and granites are even corundum normative and therefore peraluminous . Their A / CNK ratio is between 0.85 and 1.2 and thus indicates a metaluminous to peraluminous character. Normative olivine occurs in diorites and gabbros. The TiO ₂ content is quite high in the mafic members, as is P ₂ O ₅ . CaO and MgO are very low in concentration and only important in ultramafites and gabbro. The iron oxide and MnO contents, which are extremely low in granite, are comparable.

Trace elements

Table with trace elements :

Trace element ppm	Ultramafic inclusion	Gabbro inclusion	Diorite	Monzonite	Syenite	Granodiorite	Granodiorite porphyry	granite	Syenogranite
Cr		130	6th	9		6th		5
Ni	447	64	0	7th	76	3	50	0	54
Sc		22nd	10	4th				1
Zr	120	241	252	426	211.7	217	182.3	135	110.3
Nb	23	39.0	47.0	18.0	32.1	14.4	32.5	19.0	46
Nd	18.8	32.43	37.36	36.64	19.8	1.84	28.6	14.82	16.6
Rb	30th	55	81	121	165.3	119	163.9	222	244.2
Sr	335	534	582	349	236.1	362	287.7	168	76.2
Ba	94	130	387	582	295.2	368	335.7	332	130.6
Th	3.7	2	5	10	24.03	24	23.69	3	37.84
Co		16
V	205	193	113	23	25th	27	24	5	18th
La	16.3	36.86	38.11	78.77	35.3	34.01	43.2	25.83	21.2
Ce	35.6	68.46	75.99	110.60	64.7	53.51	84.7	40.37	44.7
Sm	4.7	6.80	8.09	5.71	3.4	3.22	4.5	3.09	3.6
Eu	1.32	1.54	1.91	1.27	0.82	1.05	1.07	0.56	0.29
Yb	1.2	2.60	2.89	1.70	1.7	1.12	2.4	1.51	3.8

The transition metals chromium , nickel , scandium and vanadium are still very highly concentrated in the ultramafites and gabbros, only to then sink into practically insignificance in the other rock limbs. The accumulation of alkalis and incompatible elements , such as barium , zircon and the LREE lanthanum and cerium , reaches a climax in monzonite, which is shifted towards diorite in the case of the remaining rare earths . The LREE / HREE ratio is quite low in the mafic members (suggesting a common mantle source), but much higher in monzonite, granodiorite and granite. All rocks manifest a clear fractionation of the LREE ((La / Sm) _N = 2.38 to 8.48), especially in the acidic terms. The HREEs are only indistinctly fractionated in the Mafites ((Gd / Yb) _N = 0.75 to 2.81) and in the acidic members hardly at all ((Gd / Yb) _N = 0.69 to 1.34 ). With the exception of gabbro, all rocks have a moderate to strong, negative europium anomaly (Eu / Eu * = 0.24 to 0.99), which is more pronounced in the acidic limbs. Positive europium anomalies (Eu / Eu * = 1.10 to 2.03) only occur in some syenite porphyries and syenogranites.

Elements with low field strength ( LFSE ) or LILE such as barium, potassium and sodium are enriched, especially in monzonite and granodiorite. The HFSE element thorium also shows enrichment in the syenogranite.

Isotope ratios

Isotope ratio	Gabbro inclusion	Diorite	Monzonite	Granodiorite	granite
( 87 Sr / 86 Sr) i	0.70313	0.70374	0.70525	0.70475	0.70473

The initial ratios of the strontium isotopes are generally still relatively low with a maximum value for monzonite of 0.70525. They show a significant increase from gabbro to monzonite and then stabilize from monzonite to granite. This indicates AFC processes (assimilation coupled with fractional crystallization) in the mafic rocks. After the residual melts with monzonite had become more and more rocky (ie more acidic), practically only fractional crystallization prevailed . De Paolo and colleagues (1992) and Reiners and colleagues (1995) also drew this conclusion.

Petrogenesis

At first glance, the rocks of the Karawanken granite pluton are a prime example of a Bowen differentiation series , which is likely to be unique in the Eastern Alps. Their composition ranges from Olivingabbro to Syenogranit. However, on closer examination of the field data and the petrological and geochemical analyzes, their differentiation is not the result of a single crystal fractionation process nor of a simple mixing process. Only the mafic and acidic end links can be related to each other through consistent crystal fractionation. Rather, rocks with an intermediate composition are the result of an interaction between the mafic and acidic magma terminal.

The gabbro slices contained show that a gabbroic precursor magma must have existed before the dioritic one. This was followed by the granitic magma surge, which partially penetrated the diorite, reshaped it and partially dissolved it. This resulted in mixed or hybrid rocks. In the final stage of the intrusion, a series of aplites, pegmatites and lamprophyren formed . Exner (1972) interpreted the gastric thrusts gabbro-diorite-granite as cogenetic. He sees the included inclusions as clear signs of the spatial mixing of magmas ( English magma mingling ) and possibly also for a chemical mixing process (English magma mixing ). The hybrid rocks monzonite, monzodiorite and monzogabbro are likely to be due to this.

The investigations by Miller and colleagues (2011) make it clear that the Karawanken granite pluton emerged from a multiphase magma sequence, which combined the processes of crystal accumulation (cumulate), fractional crystallization and assimilation with spatial and physical mixing. The Mafites bear the geochemical signature of intraplate rocks and point to anorogenic magmatism of an enriched mantle spring in the expansion regime. The mafic melts provided the heat required to melt the crust. This in turn resulted in granitic melts, whose high Fe / Fe + Mg ratios also indicate an intraplate environment.

The geochemical characteristics of the Karawanken granite pluton suggest a source region of mantle rock , which was enriched in both LILE and HFSE . The simultaneous magmas in the Dolomites , however, originate from a mantle source that was modified by subduction processes in the Paleozoic. The Dolomites belonged to a different microplate and were only united with the Karawankenterran in the Middle Carboniferous. However, both magmas have in common that they can be assigned to the Central Triassic tectonic regime of transtension or extension, which had set in at the beginning of the Mesozoic rift in the southern Alpine, Austroalpine and Dinaric regions.

Age

Mineral dating has given the Karawanken granite pluton ages between 244 and 224 million years, e.g. hornblende 244 ± 9 million years, sphen (titanite) 230 ± 5 million years and biotite 227 ± 7 and 224 ± 9 million years. A back calculation of the strontium initial ratios in biotite produced 221 ± 6 million years. Scharbert (1975) determined the granodiorite to be 224 ± 9 or 216 ± 9 million years. The intrusion ages are therefore between 244 and 216 million years, which roughly corresponds to the Ladinian / Carnian period.

Stratigraphic evidence for the higher age of the Karawanken granite pluton was provided by the discovery of Isailović and Milićević near Ravnah nad Šoštanjem in 1964 , who discovered the inclusion of a metamorphic rock block in the Karawanken tonalite pluton, which was penetrated by granite.

More recent studies by Genser and Liu (2010) using the uranium-lead method on zirconium and sphene on granite have shown two age clusters at 300 to 280 and at 250 to 240 million years. The latter cluster was also confirmed by Miller and colleagues (2011). These authors therefore interpret the latest data set as follows:

• Ages between 500 and 450 million years indicate a relic magmatic event in the Ordovician .
• The actual intrusion of the Karawanken granite pluton occurred in the Permian between 300 and 280 million years.
• By around 245 million years, the intrusion had cooled to 550 ° C.

A comparable alkaline, Permotriassic magmatism can also be found in the western Alps in Briançonnais, in the Acceglio zone and in the magmatic complex of Monzoni / Predazzo; this magmatism had immediately preceded the breakup of Pangea . According to Bonin and colleagues (1987), these alkaline deposits form the Western Mediterranean Province .

The Western Mediterranean Province was associated on the one hand with the Variscan-postorogenic consolidation of Europe, which contained fragments of Gondwana docked at Laurasia , and on the other hand with the forerunner stages of the ocean basins of the Mesotethys , which had emerged from the Paleotethys and now spread westward within Gondwana. The Triassic is characterized in the Mediterranean area between 245 and 200 million years from this process of expansion, which was accompanied by the development of a huge rift system . At that time, the volcanic / plutonic complexes were made possible along deep lateral shifts in the rift.

Individual evidence

1. ^ R. Cliff, H. Holer and D. Rex: The age of the Eisenkappel granite, Carinthia and the history of the Periadriatic lineament . In: Negotiations of the Federal Geological Institute . 1975, p. 347-350 .
2. ↑ A. Hinterlechner-Ravnik: Kontaktnometamorfne Kamenine v okolici Črne pri Mežici . In: Geologija . tape 21 . Ljubljana 1978, p. 77-80 .
3. ↑ ^{a b} D. Visonà and A. Zanferrari: Some constraints on geochemical features in the Triassic mantle of the easternmost Austroalpine-South Alpine domain: evidence from the Karawanken pluton (Carinthia, Austria) . In: International Journal of Earth Sciences . tape 89 , 2000, pp. 40-51 .
4. ^ A. Wölfler, W. Kurz, H. Fritz and K. Stüwe: A new view on lateral extrusion in the Eastern Alps and the linkage to Mediterranean plate tectonics . In: Journal of Alpine Geology . tape 52 , 2010, p. 255-256 .
5. ↑ Christof Exner: The geological position of the magmatites of the periadriatic lineament . In: Negotiations of the Federal Geological Institute . 1976, p. 3-64 .
6. ↑ ^{a b} Meta Dobnikar, Tadej Dolenec, Nina Zupančič and Breda Činč Juhant: The Karavanke Granitic Belt (Slovenia) - a bimodal Triassic alkaline plutonic complex . In: Switzerland. Mineral. Petrogr. Mitt. Band 81 , 2001, p. 23-38 .
7. ↑ E. Faninger and I. Štrucl: Plutonic emplacement in the eastern Karawanken Alps . In: Geologija . tape 21 , 1978, p. 81-87 .
8. ^ OT Rämö and I. Haapala: One hundred years of rapakivi granite . In: Mineralogy and Petrology . tape 52 , 1995, pp. 129-185 .
9. ↑ ^{a b} J. D. Blundy and RSJ Sparks: Petrogenesis of mafic inclusions in granitoids of the Adamello Massif, Italy . In: Journal of Petrology . tape 33 , 1992, pp. 1039-1104 .
10. ↑ A. Hinterlechner-Ravnik: Ultramaficni vkljucki v granitu Crne na Koroskem v Sloveniji . In: Geologija . tape 31,32 , 1988, pp. 403-414 .
11. ↑ ^{a b} M. J. Hibbard: The Magma Mixing Origin of Mantled Feldspars . In: Contrib. Mineral. Petrol. tape 76 , 1981, pp. 158-170 .
12. ↑ PW Reiners, BK Nelson and MS Ghiorso: Assimilation of felsic crust by basaltic magma: thermal limits and extents of crustal contamination of mantle-derived magmas . In: Geology . tape 23 , 1995, pp. 563-566 .
13. ^ Christof Exner: Geology of the Karawanken plutons east of Eisenkappel, Carinthia . In: Communications of the Geological Society Vienna . tape 64 , 1972, p. 1-108 .
14. ^ ^{A b} C. Miller, M. Thöni, W. Goessler and R. Tessadri: Origin and age of the Eisenkappel gabbro to granite suite (Carinthia, SE Austrian Alps) . In: Lithos . tape 125 , 2011, pp. 434-448 , doi : 10.1016 / j.lithos.2011.03.003 .
15. ↑ H. Lippolt and R. Pidgeon: Isotopic mineral ages of a diorite from the Eisenkappel intrusion, Austria . In: Z. Naturforsch. 29a. Wiesbaden 1974.
16. ↑ S. Scharbert: Radiometric age data of intrusive rocks in the Eisenkappel area (Karawanken, Carinthia) . In: Negotiations of the Federal Geological Institute . 1975, p. 301-304 .
17. ^ S. Isailović and M. Milićević: Geološko kartiranje granita Črne na Koroškem i obodnih tvorevina . In: Zavod za nuklearne sirovine . Beograd 1964, p. 53 .
18. ^ J. Genser and X. Liu: On the age of the Eisenkappel granites . In: Journal of Alpine Geology . tape 52 , 2010, p. 121-122 .
19. ↑ ^{a b} B. Bonin, B. Platevoet and Y. Vialette. Y .: The geodynamic significance of alkaline magmatism in the western Mediterranean compared with West Africa . In: Geol. J. Band 22 , 1987, pp. 361-387 .