Gemericum (GEM)
compiled:
S.W. Faryad (2002)
completed:
==== ==== ====
Definition
Age of Protolith, Geochemistry
Lithology, Mineralogy, Metamorphic Grade
Thermobarometry
Geochronology
Structural Evolution
Summary
Bibliography
Links
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Definition
The Gemericum
unit with basement rocks and late Paleozoic cover sequences represent the most
inner tectonic unit of the Central Western Carpathians. It consists mostly of
greenschist facies rocks, which are partly intruded by Permian Granite. Amphibolite
facies rocks form small tectonic slices in the N, NE part of this unit.
Geographic Position
The
Gemericum called also as eastern part of the Slovak Ore Mts. is situated in the
SE part of Slovakia, between Košice in the east and Dobšina in the northwest.
Maps
Geological
map of the eastern part of Slovak Ore Mts.: 1:50000 (Bajaník etl
al., 1984), 1:500,000 (Lexa et al., 2000).
Boreholes
Most of basement rocks
in the Gemericum are exposed on surface. They were penetrated by many deep
boreholes and mains. The most important borehole occurred in basement rocks
were MPV-8 at Mníšek nad Hnilcom (Grecula and
Kobulský., 1981) and S- Sulova
north from Rožňava (Snopko et al., 1980).
The Gemericum overthrust the Veporicum along the
Lubenik tectonic zone in the West and along Margecany tectonic zone in the
northwest. The Rožňava tectonic line represents the southern border of the
Gemericum, but mostly it is overthrusted by the Silica Nappe and by the Meliata
unit.
Subunits
Based on lithology and metamorphism four subunits
form from bottom to top can be distinguished in the Gemericum:
-
Gelnica
Group, representing most part of basement rocks
-
Rakovec
Group, forming narrow rim along the north-eastern and northern parts of the Gemericum.
-
Klátov
Group (Gneiss-amphibolite complex), which forms tectonic, slices on the Rakovec
Group.
-
Late
Paleozoic sequences overlay all three groups along borders around of the
Gemericum.
Correlation
The early Paleozoic of
the Gemericum, mainly the Gelnica group is lithologically correlated with
Greywacke zone in the eastern Alps (Maheľ, 1986). Abonyi (1971) considers
correlation of some lithologies of the Rakovec group with the Ochtiná
formation, situated along western boundary of the Gemericum. Possible
correlation of the Ochtina formation and the Rakovec group with the Voitsch
unit in the Eastern Alps is considered
by Neubauer and Vozárová (1990).
Based
on biostratigraphical investigations (Snopková and Snopko, 1979, Čorna and
Kamenický, 1976), mainly on foraminifers (Vozárová et al., 1998), the Gelnica
sedimentary sequences indicate Ordovician to early Silurian age. The Gelnica
Group is represented by thick sequences of flysch sediments that associate with
volcanic rocks of ryholite and dacite composition. They represent mostly
primary tuffs, rarely lavas and subvolcanic varieties. Small amounts of
carbonate rocks with black schals (lydite) and mafic and ultramafic volcanic
are also present.
A
middle Devonian to lower Carboniferous age for the Rakovec Group and Ochtina
Formation is considered according to biostratigraphica studies of Snopková and
Snopko, (1979) and (Kozur et al., 1976). The most common rocks of the Rakovec
Group are metabasites and clastic metasediments. The metabasites derived mostly
from basalts, basaltic tuffs with minor amounts of gabbros or dolerite.
According to geochemical composition the mafic rocks of the Rakovec and Gelnica
Group represent different varieties of N-MORB, E-MORB/OIT and CAB (Ivan, 1994).
The
Klátov group consists of amphibolite and gneiss with local occurrences of
marble and serpentinites. There is no
evidence on Protolith age of this Group. Geochemically the metabasites has MORB
composition (Bajaník, 1981; Hovorka and Ivan,
1985)
The
late Paleozoic sequences (Upper Carboniferous and Permian) are represented by
clastic sediments with varying amounts of volcanic rocks of ryholite and
locally of basaltic composition (Vozárová and Vozár, 1988).
Lithology, Mineralogy, Metamorphic Grade
Metamorphic
mineral assemblages in the Gelnica and Rakovec Groups indicate greenschist
facies conditions.
Metabasites
A
relic igneous diopside was found in several localities from both of the Gelnica
and Rakovec Groups. The most common metamorphic minerals in metabasites are
albite, epidote, actinolite and titanite (Faryad, 1991). Some metabasites
contain also stilpnomelane and biotite. Calcite is usually present in
actinolite-free varieties. Metadolerites may contain zoned actinolite with
Al-rich cores, which is compositionally close to actinolitic hornblende. Both
Al-rich and Al-poor phases are in equilibrium, since the amphibole composition
continuously changes towards the rims of grains. Na2O contents in
amphibole are usually low (0.1 - 0.8 vol. percent). Some metabasites from the
northern part of the Gemericum contain Na-rich actinolite or Na-Ca amphibole of
taramite composition. Mineral coexisting with taramite are albite, epidote,
Ca-garnet, titanite and biotite (Hovorka et al., 1988; Faryad and Bernhardt,
1996). Coarse grains of taramite are weakly zoned and reveal a decrease of Al
and an increase of Fe3+ from core to rim.
The
epidote composition mostly depends on the bulk rock composition; its al =
Al/(Al+Fe3+) ratios are 0.20-0.30. Fe-rich epidote, with al = 0.4 is
found in some Fe-rich rocks. Accessory allanite was also found in metabasite.
Garnet
from taramite-bearing rocks occurs in pseudomorphs of albite after calcic
plagioclase. It is rich in Ca, with an average composition of Grs73,
And18, Sps2, Alm2, and Py0.2. Some
garnet crystals show pronounced zoning; the grossularite content decreases and
andradite increases from core (Grs72, And20) to rim (Grs44,
And54). The maximum MgO content, analyzed in a garnet core, was 0.6
wt percent.
Apart from retrograde biotite, replacing actinolite in some metabasites,
prograde biotite associates with taramite, garnet, albite and epidote in the
Rakovec locality. Compared to retrograde biotite, it is rich in Mg with an XMg
of about 0.47. Composition of chlorite is strongly related to the whole rock
composition. Its XMg content is 0.30-0.48. Plagioclase is usually an
albite with a maximum CaO content of 0.8 wt percent.
Metamorphosed acid to
intermediate volcanic rocks
In
addition to quartz, the common relic magmatic phases are phenocrysts of
feldspars. Hornblende, corresponding to magnesio-hornblende, and well-preserved
phenocrysts of biotite are found in metadacite and metarhyolite from the
central part of the Gemericum, near Rožňava (Faryad, 1991). Metamorphic
minerals are quartz, albite, white mica, chlorite and, rarely, biotite. K-rich
rocks may also contain microcline. Igneous plagioclase and K-feldspar are
replaced by white mica, albite and microcline. Since pyroclastic varieties are
well foliated, lavas and subvolcanic members are mostly spared from
deformation. White mica composition depends on the whole rock chemistry.
Phengite with Si = 3.3 atom/formula unit (a/f.u.) occurs in metadacite, but
K-rich metarhyolite may contain muscovite. Epidote or calcite is found in
dacite or ryhodacite varieties. Some Al-rich tuffaceous rocks (probably a
mixture of volcanic and sedimentary rocks) contain muscovite, chloritoid
(Varga, 1973) and pyrophyllite (Korikovsky et al., 1992; Faryad, 1995). The
presence of chloritoid is mostly restricted to the southern and eastern parts
of the Gemericum. It has high Fe contents (Fe2+ /(Fe2+ +
Mg) = 0.87-0.88).
Kyanite
and andalusite, the latter related to thermal overprint by granitoid magma,
were observed in the central part of the Gemericum (Faryad and Dianiška, 1992).
Both kyanite and andalusite are partly replaced by muscovite. Green biotite can
be observed in the area of relatively deep erosion or in some boreholes and
mines. In addition to relatively higher metamorphic conditions, the appearance
of biotite in volcanic rocks is favored by the whole rock composition, since
metapelites adjacent to volcanic rocks lack biotite. Abundant biotite occurs in
the contact zones of the Gemericum granite bodies. Thermal and hydrothermal
recrystallization in contact zones of granites resulted in a gneiss-like
appearance of some well-foliated metavolcanic rocks, which had been
misinterpreted as gneisses in the past.
Metapelites and
metapsammites
The most common rocks of sedimentary origin
are phyllites, which originated from sandstones, greywackes, pelites and black
shales. Carbonate rocks and lydite (a rock consisting of quartz and organic
matter) form intercalations in black shales. Metapelites and metapsammites are
characterized by monotonous metamorphic mineral assemblages that contain
quartz, white mica, chlorite and rarely also albite. In the southern and
eastern parts of the Gemericum, some phyllites may also contain chloritoid.
According to Varga (1973) chloritoid was formed during Alpine metamorphic
overprint. Almandine-rich garnet was observed in the eastern and northern parts
of the Gemericum. In the first place it was found near to granite, where it is
associated with chlorite, quartz and white mica. Textural relations show that
it was formed during regional metamorphism. In the second place, garnet occurs
in metapelites near the tectonic zone under the Gneiss-amphibolite complex.
Garnet is associated with quartz, albite and pseudomorphs of chlorite after
biotite.
White
mica is mostly phengite in composition and it has a Si content of 3.15-3.30. A
low- Si content for white mica is, however, assumed based on the b0 values
obtained by Sassi and Vozárová (1987) and Mazzoli et al. (1992). Paragonite was
detected by powder diffraction analyses. Chloritoid has a composition similar
to that in metavolcanics and it is rich in Fe. Biotite and/or andalusite,
occurring in the central part of the Gemericum
(Faryad and Dianiška, 1992), are related to the thermal heating of
Permian granite intrusion.
Metamorphic rocks of
specific composition
Carbonate
rocks occur mostly in the central part of the Gemericum, where they are
associated with black phyllites. Calcite marbles are common, but some magnesian
marbles or magnesites also occur. In
addition to calcite, magnesite and dolomite, the magnesian marbles contain,
quartz, white mica, chlorite and talc. In contact aureoles of granite, some
carbonate rocks are converted to skarn, which contain Ca-amphibole, pyroxene
(diopside-hedenbergite and grossularite- andradite-rich garnet (Faryad and
Peterec, 1987.
Mn-rich
carbonate rocks that underwent greenschist facies metamorphism were
investigated at three localities in the central part of the Gemericum (Faryad,
1994). They contain rhodonite, calcite, Mn-calcite, spessartite-rich garnet
(Sps60-90, Grs10-30, Alm0-15) pyroxmangite,
knebelite, biotite, phengite, chlorite, manganoan actinolite and tirodite. As
retrograde phases, these rocks may have caryopilite and manganpyrosmalite.
Grunerite
with biotite is found in iron quartzite near Helcmanovce, north of Smolník,
where stratobound pyrite deposits occur (Faryad, 1991). The iron quartzite,
forming small lenses in metavulcanite, was penetrated by a drill hole.
The Gneiss-amphibolite complex = Klátov nappe) Metamorphic
minerals in amphibolites are amphibole, plagioclase and partly garnet. In
addition to plagioclase and quartz the gneisses may contain amphibole, garnet
and biotite (Rozložník, 1965, Dianiška and Grecula, 1979, Hovorka et al., 1984,
Faryad, 1986, 1990). Most amphiboles from garnet amphibolite correspond to
magnesohornblende-tscermakite, but some amphiboles have composition of
edenite-pargasite. The total Al2O3 content varies between
8-12 mol %. Maximum NaM4 content in tschermakite is 0.4 a.f.u.
Garnet in amphibolite has composition Alm61-66, Py13-17,
Grs10-20, and Sps2-8. It shows weak zonation with
decrease of Fe, Mg and increase of Ca toward rim. Some garnet grains are rimed
by grossularite-rich garnet that were probably formed by Alpine low-grade
overprint in this unit. Plagioclase from amphibolites is mostly replaced by
albite and epidote/zoisite, but relic grains may have up to 32 mol % anorthite
content.
The
gneisses consist mostly of plagioclase (An20-32) and quartz with varying amounts of one or
more of the minerals: biotite, garnet amphiboles (magnesiohornblende and
locally cumingtonite) and muscovite. An occurrence of amphibolite and gneiss,
overprinted by high-pressure low-temperature metamorphism was described from
Rudník (Faryad, 1988), but their genetic relations to gneiss-amphibolite
complex are not clear.
Ultramafic
rocks adjacent amphibolites consist mainly of antigorite with small amounts of
tremolite, Mg-chlorite, talc and relics of brown spinel.
Thermobarometry
The polymetamorphic
character of the Gelnica and Rakovec Groups make difficult to distinguish
Pre-Alpine and Alpine mineral assemblages. In addition some rocks in the
central part of the Gemericum were affected by contact metamorphism and
hydrothermal alteration due to Permian granite intrusion.
Pre-Alpine Metamorphism:
1.
Gelnica and
Rakovec Groups
Pre-Alpine
metamorphic minerals preserved in some unfoliated massive rocks are white mica
and biotite (in ryholite), actinolite and epidote (in dolerite) and rhodonite,
pyroxmangite and knebelite (in Mn-carbonates). P-T conditions estimated for
these minerals range between 350 and
450 oC at 3-5 kbar (Faryad, 1991,1994, 1997, Vozárová, 1998). Higher
pressure and temperature (400-480 oC at 7-10 Kbar) were estimated for the Rakovec Group
for taramite-bearing assemblage (Faryad et al., 1999). Radvanec (1999) reported
a presence of jadeite from this rock that suggest pressure corresponding to
blueschist facies conditions.
2.
Klátov
Group
P-T
conditions calculated using mineral composition and various geothermobarometric
methods for amphibolites and gneisses from different localities are 500-700 °C
and 0.7-1.0 GPa (Faryad, 1990)
Mineral observed
in pelitic rocks near contact to granite are andalusite, corundum,
biotite, muscovite and pseudomorphs
after cordierite. Mafic and some carbonatic rocks contain clinopyroxene of hedenbergite
composition Grossularite/ andradite garnet and amphibole. Chlorite and biotite
spots are common feature of thermal overprint in metapelites.
P-T
conditions of Alpine metamorphism in the basement rocks of the Gemericum were estimated
according to metamorphic mineral assemblages in Permian metagranites and late
Paleozoic cover sequences (Faryad and Dianiška, 1999). The metagranites are
characterized by the presence of phengite (Si = 3.3 a.f.u), chlorite, albite,
microcline and rarely also garnet with high grossularite (Grs45-50)
and almandine contents. Some whiteschists, occurring in contact zone of
granites, contain relic corundum, andalusite and kyanite with muscovite.
Metamorphic minerals in the Permian cover sequences are white mica of
phengite-muscovite composition and chlorite. Actinolite, epidote and albite ca
be found in some upper Carboniferous
metabasites. P-T conditions of Alpine overprint in the Gemericum, calculated
using mineral composition in metagranites and estimated based metamorphic
mineral assemblages in the late Paleozoic rocks, are 0.5-07 GPa at 330-350 °C.
The early
Paleozoic rocks in the western and southern part of the Gemericum are
characterized by the presence of chloritoid (XMg = 0.08-0.15) that
associates with phengite, chlorite and locally with pyrophyllite (Varga, 1973,
Korikovsky et al., 1985, Faryad, 1997). This mineral assemblage is mostly
interpreted as result of Alpine overprint, which extensively affected eastern
part of the Veporicum at contact with Gemericum.
Geochronology
Gelnica Group
|
|
Rock type |
Locality |
Mean |
Range (n) |
Source |
|
K/Ar white mica |
phyllite |
Smolník |
148 |
(1) |
1 |
1-Cambel
et al (1980),
Rakovec
Group
|
|
Rock type |
Locality |
Mean |
Range (n) |
Source |
|
K/Ar white mica |
mylonite |
Dobšina |
227 |
(1) |
1 |
|
K/Ar white mica |
mylonite |
Rudňany |
201 |
(1) |
1 |
1-Cambel
et al (1980)
Klatov
Group
|
|
Rock type |
Locality |
Mean |
Range (n) |
Source
|
|
K/Ar
amphibole |
amphibolite |
Dobšina |
357, 338 |
(1) |
1 |
|
K/Ar
amphibole |
amphibolite |
Klátov |
262±14 |
(1) |
1 |
|
K/Ar
amphibole |
amphibolite |
Klátov |
391±18, 448±23, 337±16 |
|
2 |
|
K/Ar
amphibole |
amphibolite |
Rudňany |
324±9, 320±5, 281±9 |
|
3 |
|
K/Ar
amphibole |
amphibolite |
Ochtiná |
340±27 |
(1) |
4 |
|
K/Ar
amphibole |
|
|
|
|
|
1-Cambel et al (1980), 2-Kantor, 1980,
Kantor et al., 1981, 4- Kantor Ďurkovičová, 1980.
Beside
Permian Rb/Sr whole rock (Kovach et al., 1986) and some K/Ar ages of muscovite
from granite, many K/Ar ages from biotite and K-feldspar yielded Alpine age of
98-130 Ma (Kantor and Rybár, 1979).
Structural Evolution
Structural
analyses from the Rakovec Group (Bajaník, 1968, Konečný, 1969, Rozložník
and Sasvári, 1985) indicated northern dipping of primary foliation that
reflects a general southern vergency of the nappe. According to Rozložník and
Sasvári (1985) the Rakovec nappe and
overlaying Gneiss-amphibolite complex are characterized by bedding parallel to
foliation that dips to NE. Furthermore, Variscan folding (F1) with
general southwards vergency was recognized in these rocks by Rozložník et al.
(1981). The Upper Carboniferous sediments which cover the Rakovec nappe and the
Gneiss amphibolite complex are characterized by weak foliation and folding
along the NE-SW axes. Some amphibolite varieties are characterized by planar
compositional layers that consist mostly of plagioclase and quartz. Considering
the relationships between the Upper-Carboniferous and basement rocks, the
structural data from the Rakovec nappe and Gneiss-amphibolite complex suggest
Variscan south vergent thrust tectonics in the northern and eastern parts of
the Gemericum.
The
most important tectonic system in the Gemericum is the southwards dipping
thrust zones and cleavage, which cross cut the primary foliation in the
basement rocks. The cleavage is mostly assumed to be formed during Alpine
event, since it occurs also in the late Paleozoic and Mesozoic rocks. Some
cleavage can be however of Pre-Alpine age that related to axial planar
foliation of F1 folds in the Rakovec rocks. In the
Gneiss-amphibolite complex, the southwards dipping structures (parallel to
cleavage) are represented by thrust faults and mylonite zones.
Summary
The
Gemericum is a composite of early Paleozoic basement groups with late Paleozoic
cover sequences. The Pre-Alpine basement, representing primary
volcano-sedimentary sequences of Gelnica and Rakovec Groups underwent Variscan
greenschist facies condition Relatively higher pressures between
greenschist-blueschist facies conditions are indicated by the presence of Na-Ca
amphibole in Rakovec Gorup in the norther part of the Gemericum. Amphibolite
facies rocks of the Klátov Group form slices on the greenschist facies Rakovec
Group. The Gelnica and partly Rakovec group rocks were thermally affected by
Permian granite intrusion.
Both
early Paleozoic basement and late Paleozoic cover sequences suffered Alpine
overprint in very lo- to low-grade conditions. This metamorphism related to
collisional event, which was occurred after subduction of the Meliata oceanic
basin.
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