www.geologicacarpathica.sk
GEOLOGICA CARPATHICA, DECEMBER 2009, 60, 6, 463—483 doi: 10.2478/v10096-009-0034-z
Introduction
The Pieniny Klippen Belt (Fig. 1) is a narrow, tectonically
complicated zone of the Western Carpathians, forming the
boundary between their internides and externides. The zone
represents a melange of various paleogeographic-tectonic
units coming from the Central Western Carpathians and from
the independent Oravic Superunit which dominates the Pieniny
Klippen Belt. The shallowest Oravic unit is the Czorsztyn
Unit which is considered to be paleogeographically located on
a swell or ridge (Fig. 2). Its sedimentary record is known from
the Hettangian till the latest Cretaceous. Shallow-marine de-
posits dominated the Bajocian to Valanginian lithostratigra-
phy of this unit (Fig. 3). After the Valanginian, a hiatus
encompassing the whole Hauterivian, Barremian and substan-
tial parts of the Aptian occurred in this unit (Aubrecht et al.
2006). Tithonian to Valanginian formations of this unit are of-
ten covered by pelagic Albian to Cenomanian red marly lime-
stones, marlstones and radiolarites (Chmielowa and
Pomiedznik Formations). The cause and character of this hia-
tus were for a long time unclear. Submarine non-deposition
and erosion were the most preferred explanations because of
Provenance of the detrital garnets and spinels from the
Albian sediments of the Czorsztyn Unit (Pieniny Klippen Belt,
Western Carpathians, Slovakia)
ROMAN AUBRECHT
1,4
, ŠTEFAN MÉRES
2
, MILAN SÝKORA
1
and TOMÁŠ MIKUŠ
3
1
Department of Geology and Paleontology, Faculty of Natural Sciences, Comenius University, Mlynská dolina G, 842 15 Bratislava,
Slovak Republic; aubrecht@fns.uniba.sk; sykora@fns.uniba.sk
2
Department of Geochemistry, Faculty of Natural Sciences, Comenius University, Mlynská dolina G, 842 15 Bratislava,
Slovak Republic; meres@fns.uniba.sk
3
Geological Institute, Slovak Academy of Sciences, Severná 5, 974 01 Banská Bystrica, Slovak Republic; mikus@savbb.sk
4
Geophysical Institute, Slovak Academy of Sciences, Dúbravská cesta 9, 845 28 Bratislava, Slovak Republic
(Manuscript received August 14, 2008; accepted in revised form June 25, 2009)
Abstract: According to earlier concepts, the Czorsztyn Unit (Oravic Superunit, Pieniny Klippen Belt, Western Carpathians)
sedimented on the isolated Czorsztyn Swell which existed in the Middle Jurassic—Late Cretaceous time in the realm of the
Outer Western Carpathians. This paper brings new data providing an alternative interpretation of its Cretaceous evolution.
They are based on heavy mineral analysis of the Upper Aptian/Lower Albian sediments of the Czorsztyn Unit. They rest
upon a karstified surface after a Hauterivian-Aptian emersion and are represented by condensed, red marly organodetritic
limestones with some terrigenous admixture (Chmielowa Formation). The heavy mineral spectrum is dominated by spinels,
followed by garnet, with lesser amounts of zircon, rutile and tourmaline. The composition of the majority of the detrital
garnets shows that they were derived from primary HP/UHP parental rocks which were recrystallized under granulite and
amphibolite facies conditions. The garnets were most probably derived directly from the magmatic and metamorphic rocks
of the Oravic basement, as the high-pyrope garnets are known to be abundant in Mesozoic sediments all over the Outer
Western Carpathians. The presence of spinels is surprising. According to their chemistry, they were mostly derived from
mid-oceanic ridge basalts (MORB) peridotites, supra-subduction zone peridotites (harzburgites) and transitional lherzolite/
harzburgite types. Only a lesser amount of spinels was derived from volcanics of BABB composition (back-arc basin
basalts). The presence of this ophiolitic detritus in the Czorsztyn Unit is difficult to explain. Ophiolitic detritus appeared in
the Aptian/Albian time only in the units which were considered to be more distant, because they were situated at the
boundary between the Central and the Outer Western Carpathians (Klape Unit, Tatric and Fatric domains). The hypotheti-
cal Exotic Ridge which represented an accretionary wedge in front of the overriding Western Carpathian internides was
considered to be a source of the clastics. In previous paleogeographical reconstructions, the Czorsztyn Unit was situated
north of the Pieniny Trough (considered to be one of the branches of the Penninic-Vahic Ocean). In the trough itself, the
ophiolitic detritus appeared as late as in the Senonian and there was no way it could reach the Czorsztyn Swell which was
considered to be an isolated elevation. The new results presented herein show that these reconstructions do not fit the
obtained data and infer a possibility that the Czorsztyn sedimentary area was not isolated in the Cretaceous time and it was
situated closer to the Central Carpathian units than previously thought. A new paleogeographical model of the evolution of
the Pieniny Klippen Belt is presented in the paper: Oravic segment was derived from the Moldanubian Zone of the Bohe-
mian Massif by the Middle Jurassic rifting which caused block tilting where most of the Oravic units were arranged north
of the Czorsztyn Swell. The Oravic segment was situated in the lateral continuation of the Central and Inner Western
Carpathians from which it was detached by later clockwise rotation. The Oravic segment was then laterally shifted in front
of the Central Western Carpathians, together with remnants of the Meliatic suture zone which represented a source for the
exotics to the Klape, Tatric, Fatric and Oravic units.
Key words: Cretaceous paleogeography, provenance, Pieniny Klippen Belt, heavy minerals.
464
AUBRECHT, MÉRES, SÝKORA and MIKUŠ
Fig. 1. Structural scheme of Slovakia (according to Lexa et al. 2000 – modified) and location of the sampling sites.
Fig. 2. Reconstruction of the paleogeographical position of the indi-
vidual Oravic units after Birkenmajer (1977, slightly modified).
the pelagic character of the overlying sediments. Detailed
studies, however, showed that the hiatus resulted from emer-
sion, erosion and karstification of the older sediments
(Aubrecht et al. 2006). The research also revealed that the
deposition of the overlying Chmielowa Formation started in
the Late Aptian in the form of red organodetritic limestones
with phosphatic stromatolites and oncoids and sandy detrital
admixtures which are locally preserved at the base of the for-
mation. Already the thin-section study revealed the presence
of spinel grains, together with some small basaltic pebbles in
465
DETRITAL GARNETS AND SPINELS FROM THE ALBIAN SEDIMENTS (PIENINY KLIPPEN BELT)
Fig. 3. Lithostratigraphic chart of the Czorsztyn Unit from Aalenian
to Albian.
these limestones, and provoked detailed heavy mineral analy-
sis which brought unexpected results with far-reaching conse-
quences in the paleogeography of the Outer Carpathians.
Studied localities and analytical methods
Seven samples from six localities were analysed for heavy
minerals: Vršatec I, Vršatec II, Horné Sŕnie (2 samples),
Lednica, Jarabina and Kamenica (Fig. 1; for the detailed loca-
tion of the sampling sites see Aubrecht et al. 2006). The average
weight of the samples was about 2 kg. To separate the sandy
siliciclastic admixture, the samples were dissolved in acetic
acid and washed by water. The fraction between 0.08 and
0.71 mm was separated by sieving. Smaller grains were
washed out because of the difficulty of determining by optical
methods. The remaining fraction underwent separation in
heavy liquids (bromoform and tetrabromethane, densities 2.8
and 2.92 respectively). The fraction 0.08—0.25 mm was stud-
ied in transmitting light, the whole fraction was also examined
by a stereomicroscope. The percentages of the heavy mineral
assemblages were determined by ribbon point counting.
Spinels and garnets were hand-picked, then mounted in epoxy
resin, polished and coated with carbon.
The spinels were analysed using a wave-dispersion (WDS)
electron microprobe at the Department of Mineralogy in the
Natural History Museum, London (UK). The microprobe used
was Cameca SX50. The following operating conditions were
used: 20 kV accelerating voltage, 20 nA beam current, beam
diameter 2—5 µm, counting time 20 seconds, ZAF corrections,
standards (n-natural, sy-synthetic) – TiO
2
(sy), CaTiO
3
(sy),
V (sy), wollastonite (n), Cr
2
O
3
(sy), Mn (sy), hematite (sy), Co
(sy), Ni (sy), ZnS (sy), Al
2
O
3
(sy), diopside (n), MgO
2
(sy).
Fe
2+
and Fe
3+
in spinels were calculated assuming an ideal
stoichiometry. The composition of garnets was determined
using a CAMECA SX-100 electron microprobe at the State
Geological Institute of Dionýz Štúr in Bratislava. The ana-
lytical conditions were 15 kV accelerating voltage and 20
nA beam current, with a peak counting time of 20 seconds
and a beam diameter of 2—10 µm. Raw counts were corrected
using a PAP routine.
Results and source rocks interpretation
Percentages of heavy minerals
In all the samples, spinels and garnets are dominant, with
lesser amounts of rutile, tourmaline and zircon (Fig. 4). In
some samples, increased numbers of tourmaline, anatase and
magnetite were recorded (Fig. 4, Table 1). Kyanite and il-
menite grains were also found in rare cases. For provenance
studies of this assemblage, chemical analyses of the two most
abundant minerals, garnet and spinel, were carried out.
Fig. 4. Diagram showing percentages of the individual heavy min-
erals in the examined samples.
466
AUBRECHT, MÉRES, SÝKORA and MIKUŠ
Chemical composition of detrital garnets and their origin
Garnets belong to a group of rock-forming minerals with
high importance for interpretations of the genesis of many
types of rocks: (1) garnets are useful in defining metamorphic
Locality
Spl Grt Zrn Rt Tur Ant Mgt
Horné Sŕnie 1
57
27
0
7
9
0
0
Horné Sŕnie 2
56
21
5
9
9
0
3
Vršatec 1
53
36
7
4
0
0
0
Vršatec 2
50
7
3
9
19
12
0
Lednica
65
12
0
14
9
0
0
Kamenica
59
28
2
4
7
0
0
Jarabina
46
31
8
9
4
2
0
Explanations: Spl — spinels, Grt — garnet, Zrn — zircon, Rt — rutile,
Tur — tourmaline, Ant — anatase, Mgt — magnetite. All symbols for
rock-forming minerals in this paper were used according to Kretz (1983).
Table 1: Percentual ratios of heavy minerals in the examined samples.
Fig. 5. Composition of the garnets from UHP/HP metamorphic conditions in the classification diagrams “pyrope-almandine-grossular” (Méres
2008). Explanations: A = field of Grt compositions from HP/UHP conditions; B = field of Grt compositions from granulite and eclogite facies
conditions; C1 = transitional field of Grt compositions from high amphibolite to granulite facies conditions; C2 = field of Grt compositions
from amphibolite facies conditions (Comment: field C2 includes many other Grts too: Grt from blue schists, Grt from skarns, Grt from serpen-
tinites, Grt from igneous rocks, etc.). No. 1—7: Source rocks of the individual garnets (see text).
Source of the garnet compositions. Right diagram: Grt from HP granulites in the Góry Sowie Mts (Polish Sudetes; O’Brien et al. 1997), Grt
from peridotites, eclogites and granulites from the Bohemian Massif (Messiga & Bettini 1990; Nakamura et al. 2004; Seifert & Vrána 2005;
Vrána et al. 2005; Medaris et al. 2006a,b; Janoušek et al. 2006, 2007; Racek et al. 2008), Grt from HP and UHP eclogites and garnet peri-
dotites from the Western Gneiss Region (WGR, Norway; Krogh Ravna & Terry 2004), Grt from kimberlites (Schulze 1997), Grt from eclogites
with inclusions of diamond (Schulze 1997), Grt from HP granulites, from UHP eclogites with inclusions of coesite and Grt peridotites from
the Saxonian Erzgebirge and Granulitgebirge (Massonne & Bautsch 2004). Left diagram: Grt from mica schists, gneisses and amphibolites
and amphibolized eclogites occurrence in the pre-Alpine basement rocks of the Western Carpathians Mts (Hovorka et al. 1987; Méres & Ho-
vorka 1989, 1991; Hovorka & Méres 1990, 1991; Korikovsky et al. 1990; Hovorka et al. 1992; Janák et al. 1996, 2001, 2007; Hovorka &
Spišiak 1997; Vozárová & Faryad 1997; Faryad & Vozárová 1997; Janák & Lupták 1997; Méres et al. 2000; Faryad et al. 2005).
conditions, (2) can be utilized for the estimation of the p-T
history of the host rock, (3) garnets are very good indicators
of their parental rock types (mafic, felsic, Mn-rich, V-rich,
Cr-rich, etc.), (4) detrital garnets are useful in paleogeography.
Natural garnets grown in various metamorphic conditions
were classified by Méres (2008; Figs. 5 and 6) in pyrope-al-
mandine-grossular and pyrope-almandine-spessartine triangle
diagrams. Three main groups were distinguished: (A) garnets
from HP/UHP (high-pressure to ultra-high-pressure condi-
tions), (B) garnets from eclogite and granulite facies condi-
tions, (C) garnets from amphibolite facies conditions, with
C1 – transitional subgroup between the granulite and am-
phibolite facies conditions and C2 – subgroup of the amphib-
olite facies conditions. These groups have been distinguished
according to their chemical compositions and inclusions.
The garnets from HP/UHP conditions displaying typical
composition Prp
< 70
Alm
~
15
Grs
~
10
Sps
< 1
Uvar
< 5
,
are homoge-
neous (only the B group and C1 subgroup have diffusion zon-
ing) and contain typical inclusions of the minerals from the
467
DETRITAL GARNETS AND SPINELS FROM THE ALBIAN SEDIMENTS (PIENINY KLIPPEN BELT)
Fig. 6. Composition of the garnets from granulite and amphibolite facies conditions in the classification diagrams “pyrope-almandine-spes-
sartine” (Méres 2008). Explanations as Fig. 5.
UHP conditions such as phengite, kyanite, coesite or dia-
mond. The garnets from eclogite facies conditions have most
commonly Prp
30—50
Alm
35—45
Grs
~
10
Sps
<1
composition and con-
tain inclusions of the minerals like omphacite, phengite, rutile,
kyanite, zoisite and Al-Cr-spinels. The garnets from granulite
facies conditions are characterized by Prp
20—30
Alm
50—60
Grs
< 30
Sps
< 2
composition and contain inclusions of minerals
such as diopside, rutile, spinel, amphibole or pargasite. The
garnets from the transitional subgroup between the granulite
and amphibolite facies conditions (C1) generally display
Prp
15—25
Alm
< 70
Grs
< 30
Sps
< 3
composition and contain inclu-
sions
of minerals typical for high-grade amphibolite facies
rocks (e.g. Cpx + Hbl+ Plg symplectites). The garnets from
amphibolite facies conditions (C2 subgroup) generally have
Prp
< 15
Alm
~
75
Grs
< 30
Sps
> 3
composition. Prograde growth zo-
nation and inclusions
of the minerals like kyanite, sillimanite,
andalusite, staurolite, chloritoide, biotite, plagioclase, amphib-
ole, K-feldspar, epidote and muscovite are typical for these
garnets. In the C2 subgroup, garnets from many other sources
integrate, for example garnets from igneous rocks (granitoids,
syenites), HP/LT metamorphic rocks, contact-metamorphosed
rocks (skarns) or from serpentinites.
Some garnet grains from the examined samples showed pre-
served euhedral crystal shape; most of the grains were suban-
gular, showing a low-grade of roundness (Fig. 7a). Some of
the analysed garnet grains bear traces of intrastratal etching.
Electron microprobe analyses of the detrital garnets (48
grains, 105 analyses) from the Vršatec I, Vršatec II, Jarabina,
Horné Sŕnie, Lednica and Kamenica localities show signifi-
cant variation in chemistry. Variation of garnet composition is
expressed in the relative proportions of the pyrope, almandine,
grossular and spessartine end member components (Table 2).
The garnets were classified according to the above mentioned
pyrope-almandine-grossular and pyrope-almandine-spessar-
tine diagrams (Méres 2008). The composition of detrital gar-
net grains shows that they can be subdivided into 7 groups,
according to their parental rocks (Fig. 8a and Fig. 8b):
(1) Garnets derived from UHP eclogites or garnet peridot-
ites (Fig. 8a and Fig. 8b field A.1). This garnet assemblage is
dominated by high pyrope (around and higher 50 mol %),
moderate almandine (30—40 mol %) and grossular (11—
17 mol %) and low spessartine components (less than
1 mol %). The garnets are relatively homogeneous due to
their high-temperature equilibration above 600—650 °C. The
garnets locally contain inclusions of Al
2
SiO
5
(kyanite,
Fig. 7–Grt 2—9).
(2) Garnets derived from HP eclogites and HP mafic granu-
lites (Fig. 8a and Fig. 8b field B.2) are also homogeneous.
These garnets are characterized by high pyrope (30—
50 mol %), moderate almandine (40—50 mol %) and grossular
(17—20 mol %) molecule and very low spessartine contents
(less than 2 mol %).
(3) Garnets derived from felsic and intermediate granulites
(Fig. 8a and Fig. 8b field B.3). These garnets are dominated
by relatively high pyrope (30—40 mol %), moderate almand-
ine (48—60 mol %), higher amounts of grossular molecules
(less than 5 mol %) and very low spessartine (less than
2 mol %). These garnets are relatively homogeneous.
(4) Garnets derived from gneisses metamorphosed under
P-T transitional to granulite and amphibolite facies condi-
468
AUBRECHT, MÉRES, SÝKORA and MIKUŠ
tions (Fig. 8a and Fig. 8b field C1.4&5). They have higher
almandine contents (60—70 mol %), lower pyrope contents
(20—30 mol %) than the granulitic garnets, but low content of
spessartine ( < 2 mol %) and grossular ( < 5 mol %). These gar-
nets are homogeneous.
(5) Garnets derived from amphibolites metamorphosed
under transitional P-T granulite to amphibolite facies condi-
tions (Fig. 8a and Fig. 8b field C1.4 & 5). They differ from the
4-group garnets by having higher proportions of the grossular
molecule (6—30 mol %) and relatively lower almandine con-
tents (45—60 mol %). These garnets locally contain inclusions
Fig. 7a. Back-scattered electron (BSE) images of the detrital garnets from the Upper Aptian/Lower Albian sediments of the Czorsztyn Unit.
(Fig. 7a) of spinel (Spl in Grt 4—12), TiO
2
(Rtl in Grt 2—10),
muscovite (Ms in Grt 2—10) and pyrite (Py in Grt 2—10).
(6) Garnets derived from gneisses metamorphosed under
amphibolite facies conditions (Fig. 8a and Fig. 8b field C2.6).
They have the highest almandine contents ( > 70 mol %), low-
est pyrope contents ( < 20 mol %) and highest contents of sp-
essartine (2—28 mol %) of the studied detrital garnets.
Contents of grossular were less than 7 mol %.
(7) Garnets derived from amphibolites metamorphosed un-
der amphibolite facies conditions (Fig. 8a and Fig. 8b
field C2.7). They differ from the group 6 by having higher
469
DETRITAL GARNETS AND SPINELS FROM THE ALBIAN SEDIMENTS (PIENINY KLIPPEN BELT)
Fig. 7b. Back-scattered electron (BSE) images of the detrital spinel, rutile, ilmenite, kyanite and zircon from the Upper Aptian/Lower Albian
sediments of the Czorsztyn Unit.
proportions of the grossular molecule (7—45 mol %) and lower
almandine contents (45—55 mol %). These garnets (together
with the garnets from the group 6) exhibit chemical growth
zoning characterized by Ca- and Mn-richer cores and Fe- and
Mg-richer rims (Fig. 7a–Grt 4—4; Table 2). Occurrence of the
growth zoning in the garnets indicates their origin in the tem-
perature field below 600 °C. The inclusions (Fig. 7a) in the
detrital garnets of the 6 and 7 groups are mainly apatite (Ap in
Grt 4—9, Grt 4—14), biotite (Bt in Grt 4—14), zoisite (Zo in
Grt 4—4), SiO
2
(Qtz in Grt 4—4) and zircon (Zr in Grt 4—10 and
in Grt 4—11). Part of the garnets belonging to this group which
has higher grossular (27—48 mol %) and spessartine contents
(3—30 mol %) was most likely derived from HP/LT metaultra-
mafites (number 7* in Table 2).
The variable compositions of the analysed detrital garnets
suggest, that the source area comprised predominantly large
complexes of the metamorphic parental rocks formed under
medium to high-grade conditions. Garnets from the rocks like
garnet peridotite, eclogite and granulite (Fig. 8a,b field A and
field B) indicate that their source area was initially metamor-
phosed under HP(UHP?)/HT conditions. Garnets from the
rocks such as gneisses and amphibolites (Fig. 8a,b field C2)
indicate the amphibolite facies metamorphism. The garnet
compositions show continuous distribution between the two
470
AUBRECHT, MÉRES, SÝKORA and MIKUŠ
Fig. 8a. Ternary diagrams
of the almandine-pyrope-
grossular ratios, classify-
ing the source rocks of the
studied detrital garnets
from Upper Aptian/Lower
Albian sediments of the
Czorsztyn Unit according
to their origin. Explanations
see Fig. 5 and Fig. 6.
end-members (represented by the fields C1 and C2). It sug-
gests that the initial HP/UHP complex of the parental rocks
was exhumed and retrogressively recrystallized under granu-
lite and amphibolite facies conditions. Population of the detri-
tal garnets (Fig. 8a,b) from Vršatec I, Vršatec II and Jarabina
localities indicates a relatively high proportion of garnets de-
rived from HP/UHP parental rocks, and suggests erosion of
the lower part of the metamorphic rock complex. Relatively
high amount of garnets from amphibolite facies conditions
found at Horné Sŕnie, Lednica and partly Jarabina localities
suggests a rock source from the upper parts of the metamor-
phic rock complexes.
Chemical composition of spinels and their origin
The spinel grains were mostly fragmented (Fig. 7b); their
roundness is low (the grains are mostly subangular). The
analysed spinels (Table 3) show some chemical variability,
mainly in the most important parameters, such as Mg# (Mg/
Mg + Fe
2+
), Cr# (Cr/Cr + Al), TiO
2
and Fe
2+
/Fe
3+
. This vari-
ability points to different sources of spinels. To distinguish the
spinels derived from peridotites and volcanics, a diagram of
TiO
2
vs. Al
2
O
3
is used (Fig. 9; Lenaz et al. 2000; Kamenetsky
et al. 2001). To estimate diversity of the original tectonic posi-
tion of ophiolites, classification of peridotites on the basis of
spinel chemistry is used (Fig. 10; Dick & Bullen 1984). On
the basis of the spinel chemistry, three main groups can be dis-
tinguished: mantle peridotite spinels, volcanic spinels and rare
altered spinels.
Peridotite spinels have variable composition resulting from
Al
2
O
3
contents, which enables us to distinguish two different
groups. The first group is characterized by increased Al
2
O
3
contents (40—56.99 mol %) and MgO contents (18.54—
19.48 wt. %). Their Cr# ranges from 10 to 30 mol % and Mg#
from 66 to 78 mol %. This composition is typical for MORB
(mid-oceanic ridge basalts) peridotites. According to Dick &
Bullen’s (1984) classification, these spinels correspond to the
I-type peridotites (lherzolites). The second group is composed
of spinels with lower Al
2
O
3
contents (12.82—26.09 wt. %) and
also lower MgO contents (9.29—14.02 wt. %). Their Cr# is
higher (51—74 mol %) and Mg# lower (47—69 mol %) than in
the first group. Such spinels correspond to SSZ peridotites
471
DETRITAL GARNETS AND SPINELS FROM THE ALBIAN SEDIMENTS (PIENINY KLIPPEN BELT)
Fig. 8b. Ternary diagrams
of the almandine-pyrope-
spessartine ratios, classify-
ing the source rocks of the
studied
detrital
garnets
from the Upper Aptian/
Lower Albian sediments of
the Czorsztyn Unit accord-
ing to their origin. Explana-
tions see Fig. 5 and Fig. 6.
(supra-subduction zone) and after Dick & Bullen (1984) they
fall within the ranges of II-type and III-type ophiolites
(harzburgites).
Spinels of volcanic origin were found rarely (only 10.6 % of
the analysed grains). They were found only at Kamenica and
Vršatec localities. The TiO
2
contents range from 0.22 to
0.44 wt. %. The Al
2
O
3
contents are more variable (15.39—
29.06 wt. %), as are Cr# (46—70 mol %) in comparison with
Mg# (55—64 mol %). The volcanic spinels chemically corre-
spond to the back-arc basin basalts (BABB).
Altered spinels were found only at the Kamenica and Vršatec
localities. Their characteristic properties are high Cr
2
O
3
con-
tents (51—63 wt. %) and FeO contents (20—24 wt. %). The
Fe
2
O
3
contents are also increased, whereas the MgO contents
have a relatively narrow range (3.56—7.95 wt. %).
Chemical composition of the peridotitic detrital spinels of
the Czorsztyn Unit can be compared with Cr-spinels from
Mesozoic ultramafic bodies of the Meliata Unit (localities:
Dobšiná, Jaklovce, Hodkovce, Sedlice etc.; Mikuš & Spišiak
2007). The first group with higher Al
2
O
3
and MgO contents,
corresponding to MORB peridotites (lherzolites), has the
same composition as the spinels from the Meliata Unit
(Fig. 9). The second group with lower Al
2
O
3
and MgO con-
tents has different composition than the spinels from the
Meliata Unit (their composition shows lower Al
2
O
3
content,
Fig. 9). Some spinels from the Vršatec I and Horné Sŕnie locali-
ties have similar composition to the spinels from the Penninic
units in the Tauern Window in the Eastern Alps (Mikuš &
Spišiak 2007).
The studied spinels can also be compared with the spinels
from recent adjacent tectonic areas of the Klape and Manín
Units (Fig. 11). Majority of them are plotted within Klape
and Manín compositional fields except for the Lednica local-
ity, which has the same composition as the spinels from the
Meliata Unit.
Paleogeographical interpretation and discussion
On the basis of previous knowledge about the heavy miner-
al assemblages in the Jurassic and Cretaceous sediments of the
Pieniny Klippen Belt, the examined heavy mineral associa-
472
AUBRECHT, MÉRES, SÝKORA and MIKUŠ
Table 2:
Representative
microprobe
analyses
of
detrital
garnets
from
the
Czorstyn
Unit.
Continued
on
next
pages
.
Lo
ca
lit
y V
ršat
ec
I
V
rša
te
c II
G
rt
N
o
.
2-
2 2-
5 2-
6 2-
7 2-
8 2-
9 2-
9
2-
1
0
2-
1
0
3-
3
3-
6
3-
6
3-
6
3-
8
3-
8
Po
si
ti
o
n
co
re
ri
m
co
re
ri
m
co
re
co
re
ri
m
ri
m
co
re
ri
m
co
re
ri
m
ri
m
ri
m
co
re
G
rt
t
y
p
e
2 2 3 7 1 1 1
5
5
7
3
3
3
5
5
Si
O
2
4
0
.2
3
3
9
.7
6
3
9
.2
6
3
7
.6
7
4
0
.9
0
4
0
.4
5
4
0
.9
4
3
8
.6
2
3
8
.4
1
3
7
.7
0
4
0
.0
7
3
9.
4
7
3
9
.7
5
3
9
.1
0
3
9
.0
0
TiO
2
0.
0
1
0.
0
2
0.
0
1
0.
1
4
0.
0
3
0.
0
8
0.
0
3
0.
0
3
0.
0
2
0.
1
2
0.
0
0
0.
0
1
0.
0
0
0.
0
7
0.
0
8
Al
2
O
3
2
1
.9
7
2
2
.3
4
2
2
.1
6
2
1
.2
6
2
2
.9
1
2
1
.2
7
2
2
.2
4
2
1
.8
4
2
1
.6
9
2
0
.8
6
2
1
.5
8
2
1.
7
5
2
1
.4
2
2
1
.8
9
2
1
.4
4
Cr
2
O
3
0.
0
1
0.
0
0
0.
0
0
0.
0
2
0.
0
7
0.
0
8
0.
0
7
0.
0
0
0.
0
0
0.
0
6
0.
0
4
0.
0
5
0.
0
2
0.
0
2
0.
0
6
Fe
2
O
3c
a
lc
1.
2
1
0.
2
2
0.
0
0
0.
0
1
0.
2
7
2.
5
0
1.
3
7
0.
0
2
0.
0
0
0.
7
6
1.
6
5
0.
8
4
1.
6
2
0.
3
1
0.
8
2
FeO
ca
lc
2
2
.3
9
2
3
.9
5
2
5
.8
2
2
9
.8
9
1
9
.1
3
1
3
.7
2
1
4
.0
8
2
5
.6
4
2
7
.5
0
3
1
.9
7
2
3
.7
7
2
7.
0
8
2
5
.5
9
2
2
.5
2
2
2
.1
5
MnO
0.
3
3
0.
5
1
0.
5
1
1.
0
4
0.
3
2
0.
3
0
0.
3
4
0.
9
9
1.
0
6
0.
4
0
0.
5
0
0.
4
6
0.
5
4
1.
0
8
0.
9
7
Mg
O
9.
3
2
1
0
.7
7
1
1
.1
3
1.
2
5
1
3
.5
0
1
4
.5
8
1
4
.6
6
5.
5
5
4.
7
6
0.
9
1
1
2
.4
6
1
0
.3
4
1
1
.3
3
4.
8
3
4.
9
5
Ca
O
6.
8
5
3.
0
6
0.
6
1
9.
3
7
4.
2
3
6.
5
8
6.
5
7
7.
5
4
6.
9
4
8.
7
3
1.
1
1
0.
9
7
0.
9
4
1
1
.3
9
1
1
.5
1
V
2
O
3
0.
0
1
0.
0
0
0.
0
1
0.
0
1
0.
0
0
0.
0
0
0.
0
0
0.
0
1
0.
0
0
0.
0
0
0.
0
1
0.
0
0
0.
0
1
0.
0
0
0.
0
0
Tot
a
l
10
2.
3
3
10
0.
6
3
9
9
.5
1
10
0.
6
4
10
1.
3
7
9
9
.5
5
10
0.
2
9
10
0.
2
3
10
0.
3
7
10
1.
5
1
10
1.
2
0
10
0.
9
6
10
1.
2
2
10
1.
2
0
10
0.
9
7
F
o
rm
u
la
n
o
rm
al
iz
at
io
n
t
o
1
2
oxygen
s a
n
d
8
ca
ti
on
s
Si
3.
0
00
2.
9
99
3.
0
01
2.
9
95
2.
9
99
2.
9
95
2.
9
9
9
2.
9
99
3.
0
00
2.
9
93
3.
0
00
3.
0
00
3.
0
00
2.
9
98
2.
9
99
Ti
0.
0
01
0.
0
01
0.
0
01
0.
0
08
0.
0
02
0.
0
04
0.
0
0
1
0.
0
01
0.
0
01
0.
0
07
0.
0
00
0.
0
01
0.
0
00
0.
0
04
0.
0
04
Al
1.
9
31
1.
9
86
1.
9
96
1.
9
92
1.
9
80
1.
8
56
1.
9
2
0
1.
9
98
1.
9
97
1.
9
52
1.
9
04
1.
9
48
1.
9
06
1.
9
78
1.
9
43
Cr
0.
0
00
0.
0
00
0.
0
00
0.
0
01
0.
0
04
0.
0
05
0.
0
0
4
0.
0
00
0.
0
00
0.
0
04
0.
0
02
0.
0
03
0.
0
01
0.
0
01
0.
0
03
Fe
3+
0.
0
68
0.
0
13
0.
0
00
0.
0
01
0.
0
15
0.
1
40
0.
0
7
5
0.
0
01
0.
0
00
0.
0
45
0.
0
93
0.
0
48
0.
0
92
0.
0
18
0.
0
47
Fe
2+
1.
3
96
1.
5
10
1.
6
51
1.
9
87
1.
1
73
0.
8
50
0.
8
6
2
1.
6
65
1.
7
97
2.
1
23
1.
4
88
1.
7
21
1.
6
16
1.
4
44
1.
4
24
Mn
0.
0
21
0.
0
33
0.
0
33
0.
0
70
0.
0
20
0.
0
19
0.
0
2
1
0.
0
65
0.
0
70
0.
0
27
0.
0
32
0.
0
29
0.
0
34
0.
0
70
0.
0
63
Mg
1.
0
36
1.
2
11
1.
2
69
0.
1
48
1.
4
76
1.
6
09
1.
6
0
1
0.
6
42
0.
5
54
0.
1
08
1.
3
91
1.
1
71
1.
2
75
0.
5
52
0.
5
67
Ca
0.
5
47
0.
2
47
0.
0
50
0.
7
98
0.
3
32
0.
5
22
0.
5
1
6
0.
6
28
0.
5
81
0.
7
42
0.
0
89
0.
0
79
0.
0
76
0.
9
36
0.
9
49
to
t.
c
a
t.
8.
0
00
8.
0
00
8.
0
00
8.
0
00
8.
0
00
8.
0
00
8.
0
0
0
8.
0
00
8.
0
00
8.
0
00
8.
0
00
8.
0
00
8.
0
00
8.
0
00
8.
0
00
to
t.
o
x
y
.
1
2
.0
00
1
2
.0
00
1
2
.0
00
1
2
.0
00
1
2
.0
00
1
2
.0
00
1
2
.0
00
1
2
.0
00
1
2
.0
00
1
2
.0
00
1
2
.0
00
1
2
.0
00
1
2
.0
00
1
2
.0
00
1
2
.0
00
G
rt
e
n
d
me
mb
er
s (mo
l %)
a
lm
a
ndi
ne
4
6
.5
4
5
0
.3
4
5
4
.9
9
6
6
.1
7
3
9
.1
0
2
8
.3
4
2
8
.7
4
5
5
.5
1
5
9
.8
6
7
0
.7
6
4
9
.6
1
5
7.
3
6
5
3
.8
5
4
8
.1
1
4
7
.4
3
py
ro
pe
3
4
.5
3
4
0
.3
4
4
2
.2
6
4.
9
2
4
9
.1
8
5
3
.6
5
5
3
.3
7
2
1
.4
1
1
8
.4
6
3.
6
0
4
6
.3
6
3
9
.0
4
4
2
.4
8
1
8
.3
9
1
8
.8
8
gr
os
su
la
r
1
7
.6
1
8.
1
7
1.
6
5
2
6
.4
5
1
0
.9
5
1
6
.1
0
1
6
.5
0
2
0
.8
9
1
9
.3
3
2
4
.0
6
2.
8
2
2.
5
5
2.
4
1
3
0
.8
1
3
0
.7
1
spessa
rti
n
e
0.
7
0
1.
0
9
1.
0
9
2.
3
2
0.
6
6
0.
6
2
0.
6
9
2.
1
7
2.
3
3
0.
9
0
1.
0
6
0.
9
8
1.
1
5
2.
3
3
2.
1
1
u
v
arov
it
e
0.
0
0
0.
0
0
0.
0
0
0.
0
2
0.
0
2
0.
0
4
0.
0
3
0.
0
0
0.
0
0
0.
0
4
0.
0
0
0.
0
0
0.
0
0
0.
0
1
0.
0
5
a
ndr
a
d
it
e
0.
6
2
0.
0
5
0.
0
0
0.
0
1
0.
0
8
1.
2
1
0.
6
5
0.
0
1
0.
0
0
0.
5
6
0.
1
4
0.
0
6
0.
1
2
0.
2
8
0.
7
5
Ca
–T
i Gt
0.
0
1
0.
0
1
0.
0
0
0.
1
1
0.
0
1
0.
0
4
0.
0
1
0.
0
2
0.
0
1
0.
0
9
0.
0
0
0.
0
0
0.
0
0
0.
0
6
0.
0
7
Fe
2
O
3calc
and
FeO
calc
calculated
from
stoichiometry,
Grt
type
=
number
of
the
parent
al
rocks
in
the
Fig.
8a,b.
473
DETRITAL GARNETS AND SPINELS FROM THE ALBIAN SEDIMENTS (PIENINY KLIPPEN BELT)
Table 2:
Continued.
Lo
ca
lit
y
Ja
rab
in
a
G
rt
N
o
.
4-
3
4-
4 4-
5 4-
6 4-
7
4-
8 4-
9
4-
1
0
4-
1
1
4-
1
1
4-
4
-1
4-
4
-2
4-
4
-3
4-
4
-4
4-
4
-5
Pos
it
ion
rim
rim
rim
rim
rim
cor
e
cor
e
cor
e
cor
e
rim
rim
→
pr
ofi
le
→
co
re
G
rt
t
y
p
e
3
7*
3 2 6
6 6 6 7
7
7*
7*
7*
7*
7*
Si
O
2
3
8
.6
4
3
7
.9
9
3
9
.2
0
3
8
.9
1
3
7
.5
8
3
7
.7
4
3
7
.7
9
3
7
.4
3
3
8
.3
6
3
8
.6
6
3
8
.7
1
3
8.
8
9
3
8
.7
7
3
9
.2
2
3
8
.4
9
TiO
2
0.
0
2
0.
1
1
0.
0
4
0.
0
4
0.
0
0
0.
0
3
0.
0
4
0.
0
5
0.
0
6
0.
0
6
0.
0
6
0.
0
8
0.
1
1
0.
0
6
0.
1
3
Al
2
O
3
2
1
.2
0
2
1
.2
7
2
1
.6
9
2
1
.6
1
2
1
.2
1
2
1
.4
9
2
1
.3
1
2
1
.0
4
2
1
.6
8
2
1
.8
9
2
1
.7
5
2
1.
7
1
2
1
.8
5
2
2
.2
3
2
1
.7
3
Cr
2
O
3
0.
0
2
0.
0
1
0.
0
5
0.
0
2
0.
0
9
0.
0
0
0.
0
7
0.
0
0
0.
0
1
0.
0
0
0.
0
0
0.
0
0
0.
0
4
0.
0
0
0.
0
0
Fe
2
O
3c
a
lc
0.
9
8
0.
2
3
0.
6
9
0.
5
7
0.
0
0
0.
0
0
0.
0
0
0.
1
4
0.
0
0
0.
0
6
0.
0
0
0.
1
4
0.
0
0
0.
0
0
0.
0
0
FeO
ca
lc
2
9
.7
9
1
9
.0
3
2
5
.4
9
2
6
.6
3
3
3
.1
3
3
2
.5
2
2
5
.9
1
3
6
.7
3
2
7
.5
6
2
8
.1
9
2
0
.5
5
2
0.
5
9
2
0
.0
8
2
0
.1
0
1
9
.2
9
MnO
1.
4
1
2.
2
3
0.
6
4
0.
5
7
3.
9
4
4.
7
3
1
2
.4
4
1.
5
9
6.
7
5
4.
7
4
1
.4
1
1.
9
7
2.
7
2
3.
3
3
3.
8
2
Mg
O
7.
0
3
1.
4
7
1
0
.4
6
7.
2
7
3.
3
6
3.
6
1
3.
0
3
2.
6
4
3.
9
5
3.
9
2
1
.4
7
1.
5
1
1.
4
8
1.
4
9
1.
5
3
Ca
O
1.
9
2
1
6
.8
7
1.
6
6
5.
0
0
1.
4
1
0.
9
5
1.
0
0
1.
3
8
3.
4
1
4.
9
3
1
6
.9
7
1
6
.6
2
1
6
.3
8
1
6
.1
7
1
5
.6
3
V
2
O
3
0.
0
1
0.
0
0
0.
0
0
0.
0
0
0.
0
0
0.
0
1
0.
0
0
0.
0
0
0.
0
1
0.
0
0
0.
0
1
0.
0
1
0.
0
0
0.
0
0
0.
0
1
Tot
a
l
10
1.
0
3
9
9
.2
0
9
9
.9
1
10
0.
6
2
10
0.
7
1
10
1.
0
8
10
1.
5
9
10
1.
0
1
10
1.
8
0
10
2.
4
4
10
0.
9
3
10
1.
5
2
10
1.
4
4
10
2.
6
1
10
0.
6
2
F
o
rm
u
la
n
o
rm
al
iz
at
io
n
t
o
1
2
oxygen
s a
n
d
8
ca
ti
on
s
Si
3.
0
0
0
2.
9
98
2.
9
99
2.
9
99
3.
0
00
2.
9
99
3.
0
00
2.
9
99
3.
0
00
2.
9
95
3.
0
03
3.
0
03
2.
9
97
2.
9
98
3.
0
02
Ti
0.
0
0
1
0.
0
06
0.
0
02
0.
0
03
0.
0
00
0.
0
02
0.
0
02
0.
0
03
0.
0
04
0.
0
04
0.
0
03
0.
0
05
0.
0
07
0.
0
04
0.
0
07
Al
1.
9
4
0
1.
9
78
1.
9
56
1.
9
63
1.
9
96
2.
0
12
1.
9
94
1.
9
87
1.
9
99
1.
9
99
1.
9
88
1.
9
76
1.
9
90
2.
0
02
1.
9
97
Cr
0.
0
0
1
0.
0
01
0.
0
03
0.
0
01
0.
0
06
0.
0
00
0.
0
04
0.
0
00
0.
0
01
0.
0
00
0.
0
00
0.
0
00
0.
0
02
0.
0
00
0.
0
00
Fe
3+
0.
0
5
7
0.
0
14
0.
0
40
0.
0
33
0.
0
00
0.
0
00
0.
0
00
0.
0
09
0.
0
00
0.
0
03
0.
0
00
0.
0
08
0.
0
00
0.
0
00
0.
0
00
Fe
2+
1.
9
3
4
1.
2
56
1.
6
31
1.
7
17
2.
2
12
2.
1
61
1.
7
20
2.
4
61
1.
8
03
1.
8
26
1.
3
33
1.
3
30
1.
2
98
1.
2
85
1.
2
58
Mn
0.
0
9
3
0.
1
49
0.
0
42
0.
0
37
0.
2
66
0.
3
18
0.
8
37
0.
1
08
0.
4
47
0.
3
11
0.
0
92
0.
1
29
0.
1
78
0.
2
16
0.
2
52
Mg
0.
8
1
4
0.
1
73
1.
1
93
0.
8
35
0.
4
00
0.
4
27
0.
3
58
0.
3
15
0.
4
61
0.
4
53
0.
1
69
0.
1
74
0.
1
70
0.
1
70
0.
1
77
Ca
0.
1
6
0
1.
4
26
0.
1
36
0.
4
13
0.
1
20
0.
0
81
0.
0
85
0.
1
18
0.
2
86
0.
4
09
1.
4
10
1.
3
75
1.
3
57
1.
3
25
1.
3
06
to
t.
c
a
t.
8.
0
0
0
8.
0
00
8.
0
00
8.
0
00
8.
0
00
8.
0
00
8.
0
00
8.
0
00
8.
0
00
8.
0
00
8.
0
00
8.
0
00
8.
0
00
8.
0
00
8.
0
00
to
t.
o
x
y
.
1
2
.0
0
0
1
2
.0
00
1
2
.0
00
1
2
.0
00
1
2
.0
01
1
2
.0
07
1
2
.0
02
1
2
.0
00
1
2
.0
03
1
2
.0
00
1
2
.0
00
1
2
.0
00
1
2
.0
00
1
2
.0
0
3
1
2
.0
08
G
rt
e
n
d
me
mb
er
s (mo
l %)
a
lm
a
ndi
ne
6
4
.4
5
4
1
.8
1
5
4
.3
3
5
7
.1
9
7
3
.7
7
7
2
.3
4
5
7
.3
4
8
1
.9
7
6
0
.1
6
6
0
.8
9
4
4
.3
6
4
4.
2
1
4
3
.2
2
4
2
.8
9
4
2
.0
3
py
ro
pe
2
7
.1
3
5.
7
6
3
9
.7
5
2
7
.8
2
1
3
.3
4
1
4
.3
0
1
1
.9
4
1
0
.5
1
1
5
.3
8
1
5
.1
1
5.
6
4
5.
7
9
5.
6
7
5.
6
9
5.
9
3
gr
os
su
la
r
5.
1
7
4
6
.9
9
4.
4
3
1
3
.5
0
4.
0
1
2.
7
0
2.
8
2
3.
9
1
9.
5
2
1
3
.5
9
4
6
.8
5
4
5
.4
3
4
4
.9
7
4
4
.1
4
4
3
.4
5
spe
ssa
rt
in
e
3.
1
0
4.
9
6
1.
3
9
1.
2
4
8.
8
8
1
0
.6
6
2
7
.8
9
3.
5
9
1
4
.9
1
1
0
.3
6
3.
0
7
4.
2
8
5.
9
4
7.
2
0
8.
4
2
u
v
arov
it
e
0.
0
0
0.
0
1
0.
0
1
0.
0
1
0.
0
1
0.
0
0
0.
0
1
0.
0
0
0.
0
0
0.
0
0
0.
0
0
0.
0
0
0.
0
5
0.
0
0
0.
0
0
an
d
rad
it
e
0.
1
5
0.
3
2
0.
0
9
0.
2
3
0.
0
0
0.
0
0
0.
0
0
0.
0
2
0.
0
0
0.
0
2
0.
0
0
0.
1
8
0.
0
0
0.
0
0
0.
0
0
Ca
-T
i Gt
0.
0
0
0.
1
5
0.
0
0
0.
0
2
0.
0
0
0.
0
0
0.
0
0
0.
0
1
0.
0
2
0.
0
3
0.
0
8
0.
1
1
0.
1
5
0.
0
8
0.
1
6
Fe
2
O
3calc
and
FeO
calc
calculated
from
stoichiometry,
Grt
type
=
number
of
the
parent
al
rocks
in
the
Figs.
8a,b,
7*
–
Grt
probably
from
HP/LT
metaul
tramafites.
474
AUBRECHT, MÉRES, SÝKORA and MIKUŠ
Table 2:
Continued
from
previous
pages.
Fe
2
O
3calc
and
FeO
calc
calculated
from
stoichiometry,
Grt
type
=
number
of
the
parent
al
rocks
in
the
Figs.
8a,b,
7*
–
Grt
probably
from
HP/LT
metau
ltramafites.
L
o
ca
lit
y H
o
rn
é
S
ŕni
e
L
ed
n
ic
a
K
a
m
en
ic
a
G
rt
N
o
.
1
3
5 7 7
1 1
2 5
2 2 5
6
7
7
P
o
sit
ion
rim
cor
e
rim
cor
e
rim
cor
e
rim
cor
e cor
e
cor
e
cor
e cor
e
cor
e core
rim
G
rt
t
y
p
e
3 6 7
7*
7
7*
7*
4
3
7
6
7 2 3
3
Si
O
2
39.
5
7
3
7
.7
3
3
7
.5
6
3
7
.9
6
37.
5
5
3
7
.5
3
3
7
.8
1
3
9
.4
0
3
9
.4
9
3
7
.69
3
8
.1
5
3
8.
1
8
3
9
.6
6
3
9
.48
3
8
.9
8
Ti
O
2
0.
0
3
0.
0
2
0.
0
9
0.
0
1
0.
0
1
0.
1
8
0.
1
6
0.
0
1
0.
0
0
0.
04
0.
0
2
0.
0
0
0.
0
0
0.
05
0.
0
8
Al
2
O
3
22.
2
9
2
1
.3
6
2
1
.2
4
2
1
.1
8
21.
1
9
2
1
.2
3
2
1
.1
3
2
1
.7
9
2
2
.2
0
2
1
.25
2
1
.5
7
2
1.
5
8
2
2
.2
1
2
2
.13
2
1
.9
3
Cr
2
O
3
0.
0
6
0.
0
0
0.
0
1
0.
0
3
0.
0
0
0.
0
3
0.
0
4
0.
0
0
0.
0
6
0.
04
0.
0
2
0.
0
8
0.
0
1
0.
02
0.
0
8
Fe
2
O
3
c
al
c
0.
0
0
0.
0
0
0.
0
0
0.
4
0
0.
1
2
0.
0
0
0.
0
8
0.
7
4
0.
0
9
0.
00
0.
0
0
0.
0
0
0.
3
7
0.
19
0.
0
0
Fe
O
ca
lc
26.
4
7
3
6
.9
3
3
1
.3
2
1
3
.6
1
22.
4
6
2
5
.6
9
2
5
.7
6
2
7
.7
8
2
6
.4
2
3
2
.82
3
4
.5
6
3
3.
0
5
2
7
.6
3
2
8
.49
2
7
.9
3
Mn
O
0.
5
2
2.
5
8
1.
5
8
1
7
.1
2
11.
6
7
6.
1
1
5.
9
9
1.
7
7
0.
5
3
1.
80
2.
0
8
0.
8
6
0.
4
1
0.
77
0.
8
4
MgO
10.
0
6
2.
5
6
1.
7
8
0.
4
0
2.
0
6
0.
65
0.
6
1
6.
7
6
9.
6
0
2.
29
4
.2
6
5.
0
6
8.
6
6
9.
23
9.
1
5
CaO
1.
8
7
0.
7
7
6.
8
2
1
0
.7
3
5.
4
3
9.
1
2
9.
7
1
4.
3
1
2.
4
4
4.
94
1
.0
4
2.
1
1
3.
0
7
1.
20
1.
1
9
V
2
O
3
0.
0
0
0.
0
1
0.
0
0
0.
0
0
0.
0
0
0.
0
1
0.
0
0
0.
0
0
0.
0
0
0.
01
0.
0
0
0.
0
0
0.
0
0
0.
00
0.
0
0
To
ta
l
100.
8
7
10
1.
9
4
10
0.
4
0
10
1.
4
4
100.
4
8
10
0.
5
6
10
1.
2
8
10
2.
5
6
100.
8
4
10
0.
8
8
10
1.
6
9
10
0.
9
2
1
0
2.
0
3
10
1.
55
10
0.
1
9
F
o
rm
u
la
n
o
rm
al
iz
at
io
n
t
o
1
2
oxygen
s a
n
d
8
ca
ti
on
s
Si
3.
0
01
3.
0
0
0
3.
0
00
3.
0
00
2.
9
99
2.
9
9
9
2.
9
99
3.
0
00
3.
0
01
3.
0
00
3.
0
00
2.
9
99
2.
9
99
3.
000
3.
0
00
Ti
0.
0
02
0.
0
0
1
0.
0
06
0.
0
01
0.
0
01
0.
0
1
1
0.
0
09
0.
0
01
0.
0
00
0.
0
03
0.
0
01
0.
0
00
0.
0
00
0.
003
0.
0
05
Al
1.
9
92
2.
0
0
1
1.
9
99
1.
9
73
1.
9
94
1.
9
9
9
1.
9
75
1.
9
56
1.
9
89
1.
9
94
1.
9
99
1.
9
97
1.
9
80
1.
982
1.
9
90
Cr
0.
0
03
0.
0
0
0
0.
0
01
0.
0
02
0.
0
00
0.
0
0
2
0.
0
03
0.
0
00
0.
0
03
0.
0
03
0.
0
01
0.
0
05
0.
0
01
0.
001
0.
0
05
Fe
3+
0.
0
00
0.
0
0
0
0.
0
00
0.
0
24
0.
0
07
0.
0
0
0
0.
0
05
0.
0
43
0.
0
05
0.
0
00
0.
0
00
0.
0
00
0.
0
21
0.
011
0.
0
00
Fe
2+
1.
6
79
2.
4
5
5
2.
0
92
0.
9
00
1.
5
00
1.
7
1
7
1.
7
09
1.
7
69
1.
6
80
2.
1
85
2.
2
73
2.
1
71
1.
7
47
1.
811
1.
7
98
Mn
0.
0
34
0.
1
7
4
0.
1
07
1.
1
46
0.
7
89
0.
4
1
4
0.
4
03
0.
1
14
0.
0
34
0.
1
21
0.
1
38
0.
0
57
0.
0
26
0.
050
0.
0
55
Mg
1.
1
37
0.
3
0
3
0.
2
12
0.
0
47
0.
2
45
0.
0
7
8
0.
0
72
0.
7
67
1.
0
88
0.
2
72
0.
4
99
0.
5
93
0.
9
77
1.
045
1.
0
50
Ca
0.
1
52
0.
0
6
6
0.
5
84
0.
9
08
0.
4
64
0.
7
8
1
0.
8
25
0.
3
51
0.
1
99
0.
4
22
0.
0
88
0.
1
77
0.
2
49
0.
098
0.
0
98
to
t.
c
a
t.
8.
0
00
8.
0
0
0
8.
0
00
8.
0
00
8.
0
00
8.
0
0
0
8.
0
00
8.
0
00
8.
0
00
8.
0
00
8.
0
00
8.
0
00
8.
0
00
8.
000
8.
0
00
tot
. ox
y.
12.
0
00
1
2
.0
0
2
1
2
.0
06
1
2
.0
00
12.
0
00
1
2
.0
1
1
1
2
.0
00
1
2
.0
00
1
2
.0
00
1
2
.002
1
2
.0
01
1
2
.0
00
1
2
.0
00
1
2
.000
1
2
.0
02
G
rt
e
n
d
me
mb
er
s (mo
l %)
a
lm
a
ndi
ne
55.
9
3
8
1
.9
1
6
9
.8
6
2
9
.9
8
50.
0
2
5
7
.4
4
5
6
.7
9
5
8
.9
4
5
5
.9
7
7
2
.83
7
5
.8
0
7
2.
4
1
5
8
.2
6
6
0
.29
5
9
.9
1
pyr
o
p
e
37.
8
8
1
0
.1
1
7.
0
7
1.
5
6
8.
1
8
2.
6
0
2.
4
1
2
5
.5
5
3
6
.2
6
9.
07
1
6
.6
5
1
9
.7
7
3
2
.5
6
3
4
.80
3
5
.0
0
g
ro
ssul
a
r
5.
0
6
2.
1
8
1
9
.4
4
2
9
.8
6
15.
4
2
2
5
.9
5
2
7
.1
9
1
1
.4
5
6.
6
0
1
4
.02
2.
9
2
5.
9
0
8.
2
1
3.
23
3.
2
5
sp
essa
rt
in
e
1.
1
2
5.
7
9
3.
5
8
3
8
.1
9
26.
3
1
1
3
.8
4
1
3
.3
8
3.
8
0
1.
1
4
4.
04
4.
6
2
1.
9
1
0.
8
8
1.
65
1.
8
3
uv
arov
it
e
0.
0
1
0.
0
0
0.
0
1
0.
0
3
0.
0
0
0.
0
3
0.
0
4
0.
0
0
0.
0
1
0.
02
0.
0
0
0.
0
2
0.
0
0
0.
00
0.
0
1
a
ndr
a
d
it
e
0.
0
0
0.
0
0
0.
0
0
0.
3
6
0.
0
6
0.
0
0
0.
0
6
0.
2
5
0.
0
2
0.
00
0.
0
0
0.
0
0
0.
0
9
0.
02
0.
0
0
Ca-
T
i G
t
0.
0
0
0.
0
0
0.
0
5
0.
0
1
0.
0
0
0.
1
4
0.
1
3
0.
0
0
0.
0
0
0.
02
0.
0
0
0.
0
0
0.
0
0
0.
00
0.
0
1
475
DETRITAL GARNETS AND SPINELS FROM THE ALBIAN SEDIMENTS (PIENINY KLIPPEN BELT)
Lo
ca
lit
y Ka
m
en
ica
Horn
é
S
ŕn
ie Led
n
ic
a
Ja
rab
in
a
V
rš
a
te
c
Sa
m
p
le
K
am
-1 H
o
s-
1
L
ed-
1
Ja
r-
1
V
rs
-1
V
rs
-2
A
n
al
ys
e
#2
#6 #1
2
#1
5 #7
#8
#1
7 #1
9
#2
1
#2
2
#2
3
#1
7 #1
9
#2
1
#5
9
#6
0
#6
4
#2
4
#2
6
#3
0
Si
O
2
0
.0
2
0
.0
0
0
.0
2
0
.0
3
0
.0
6
0
.0
5
0
.0
6
0.
06
0.
07
0.
06
0.
04
0.
03
0.
07
0.
03
0.
05
0.
09
0.
03
0.
04
0.
03
0.
02
TiO
2
0
.0
7
0
.0
3
0
.0
3
0
.0
7
0
.2
3
0
.2
2
0
.0
9
0.
08
0.
17
0.
07
0.
0
6
0.
05
0.
29
0.
06
0.
27
0.
44
0.
08
0.
12
0.
31
0.
07
Al
2
O
3
17
.3
1 56
.9
9 56
.8
0 20
.0
4
15
.4
1 15
.3
9
17
.1
2
24
.1
3
15
.1
7
44
.7
9
52
.2
9
17
.8
3 12
.8
2
25
.3
5
21
.0
4
29
.0
6
22
.2
7
10
.4
2
17
.4
4
42
.3
3
Cr
2
O
3
50
.4
5
9
.1
8
10
.3
6 49
.3
3
52
.3
7 51
.6
1
52
.0
5
44
.4
3
53
.3
1
21
.1
2
13
.2
2
50
.7
4 54
.5
7
42
.7
6
46
.1
8
36
.8
0
46
.3
3
60
.6
3
49
.2
4
24
.3
1
*F
e
2
O
3
3
.5
9
2
.2
2
1
.0
8
2
.3
5
3
.5
3
4
.3
9
2
.2
2
2.
89
0.
95
1.
68
4.
0
4
2.
39
2.
03
1.
13
4.
69
5.
08
2.
23
1.
27
4.
34
3.
27
FeO
14
.5
1
9
.8
4
11
.4
3 13
.4
9
15
.1
8 16
.2
2
14
.9
7
14
.2
8
18
.2
8
13
.5
1
9.
5
1
15
.5
8 17
.8
9
16
.5
4
14
.0
5
14
.3
5
15
.4
4
13
.5
5
16
.7
2
10
.4
3
MnO
0
.2
3
0
.1
2
0
.1
4
0
.2
3
0
.2
1
0
.2
7
0
.2
7
0.
23
0.
27
0.
14
0.
1
3
0.
25
0.
28
0.
21
0.
22
0.
21
0.
22
0.
36
0.
27
0.
15
Mg
O
12
.3
4 19
.4
8 18
.5
4 13
.4
2
11
.8
5 11
.2
7
12
.1
4
13
.4
0
9.
56
15
.6
6
19
.3
8
11
.7
5
9.
62
11
.7
1
13
.3
0
14
.0
9
12
.3
6
11
.8
9
11
.2
4
17
.6
3
Zn
O
0
.1
5
0
.2
1
0
.1
7
0
.1
3
0
.1
3
0
.1
3
0
.1
0
0.
25
0.
16
0.
24
0.
1
0
0.
16
0.
15
0.
14
0.
09
0.
07
0.
13
1.
03
0.
14
0.
16
V
2
O
3
0
.3
2
0
.0
6
0
.1
0
0
.3
2
0
.2
7
0
.2
6
0.
31
0.
29
0.
30
0.
14
0.
1
1
0.
32
0.
14
0.
34
0.
32
0.
19
0.
34
0.
26
0.
20
0.
21
Ni
O
0
.1
3
0
.4
4
0
.4
1
0
.0
7
0
.1
1
0
.0
8
0.
09
0.
08
0.
06
0.
23
0.
4
0
0.
06
0.
09
0.
16
0.
13
0.
21
0.
09
0.
04
0.
08
0.
22
Tot
a
l
99
.2
0 98
.6
6 99
.1
5 99
.5
7
99
.4
2 99
.9
5
99
.4
9
10
0.
2
2
98
.3
6
97
.7
3
99
.3
6
99
.2
1 98
.0
4
98
.4
8
10
0.
4
3
10
0.
6
8
99
.6
0
99
.7
0
10
0.
0
7
98
.8
6
Si
0.
00
1
0.
00
0 0.
0
0
1
0.
00
1
0.
00
2 0.
00
2
0.
00
2
0.
00
2
0.
00
2
0.
00
2
0.
0
0
1
0.
00
1
0.
00
2
0.
00
1
0.
00
2
0.
00
3
0.
00
1
0.
00
1
0.
00
1
0.
00
1
Ti
0.
00
2
0.
00
1 0.
0
0
1
0.
00
2
0.
00
6 0.
00
5
0.
00
2
0.
00
2
0.
00
4
0.
00
1
0.
0
0
1
0.
00
1
0.
00
7
0.
00
1
0.
00
6
0.
01
0
0.
00
2
0.
00
3
0.
00
7
0.
00
1
Al
0.
64
9
1.
76
6 1.
7
6
3
0.
73
5
0.
58
3 0.
58
2
0.
64
1
0.
86
6
0.
58
9
1.
49
2
1.
6
4
0
0.
66
9
0.
50
4
0.
92
8
0.
76
4
1.
01
5
0.
81
5
0.
40
2
0.
65
4
1.
39
5
Cr
1.
26
9
0.
19
1 0.
2
1
6
1.
21
4
1.
33
0 1.
31
0
1.
30
8
1.
07
0
1.
38
8
0.
47
2
0.
2
7
8
1.
27
8
1.
43
9
1.
05
0
1.
12
6
0.
86
3
1.
13
7
1.
56
8
1.
23
8
0.
53
8
Fe
3+
0.
08
6
0.
04
4 0.
0
2
1
0.
05
5
0.
08
5 0.
10
6
0.
05
3
0.
06
6
0.
02
4
0.
03
6
0.
0
8
1
0.
05
7
0.
05
1
0.
02
7
0.
10
9
0.
11
3
0.
05
2
0.
03
1
0.
10
4
0.
06
9
V
0.
00
7
0.
00
1 0.
0
0
2
0.
00
7
0.
00
6 0.
00
6
0.
00
7
0.
00
6
0.
00
7
0.
00
3
0.
0
0
2
0.
00
7
0.
00
3
0.
00
7
0.
00
7
0.
00
4
0.
00
7
0.
00
6
0.
00
4
0.
00
4
Su
m
B
2.
01
3
2.
00
2 2.
0
0
3
2.
01
3
2.
01
1 2.
01
1
2.
01
3
2.
01
2
2.
01
3
2.
00
5
2.
0
0
4
2.
01
3
2.
00
6
2.
01
4
2.
01
3
2.
00
7
2.
01
4
2.
01
1
2.
00
8
2.
00
8
Fe
2+
0.
38
6
0.
21
6 0.
2
5
2
0.
35
1
0.
40
8 0.
43
6
0.
39
8
0.
36
4
0.
50
3
0.
31
9
0.
2
1
2
0.
41
5
0.
49
9
0.
43
0
0.
36
2
0.
35
6
0.
40
1
0.
37
1
0.
44
5
0.
24
4
Mn
0.
00
6
0.
00
3 0.
0
0
3
0.
00
6
0.
00
6 0.
00
7
0.
00
7
0.
00
6
0.
00
8
0.
00
3
0.
0
0
3
0.
00
7
0.
00
8
0.
00
6
0.
00
6
0.
00
5
0.
00
6
0.
01
0
0.
00
7
0.
00
4
Mg
0.
58
5
0.
76
3 0.
72
8 0.
62
3
0.
56
7 0.
53
9
0.
57
5
0.
60
8
0.
46
9
0.
66
0
0.
7
6
9
0.
55
8
0.
47
8
0.
54
2
0.
61
1
0.
62
3
0.
57
2
0.
58
0
0.
53
3
0.
73
5
Zn
0.
00
4
0.
00
4 0.
0
0
3
0.
00
3
0.
00
3 0.
00
3
0.
00
2
0.
00
6
0.
00
4
0.
00
5
0.
0
0
2
0.
00
4
0.
00
4
0.
00
3
0.
00
2
0.
00
2
0.
00
3
0.
02
5
0.
00
3
0.
00
3
Ni
0.
00
3
0.
00
9 0.
0
0
9
0.
00
2
0.
00
3 0.
00
2
0.
00
2
0.
00
2
0.
00
2
0.
00
5
0.
0
0
9
0.
00
2
0.
00
2
0.
00
4
0.
00
3
0.
00
5
0.
00
2
0.
00
1
0.
00
2
0.
00
5
Su
m
A
0.
98
5
0.
99
6 0.
9
9
5
0.
98
5
0.
98
7 0.
98
7
0.
98
5
0.
98
6
0.
98
6
0.
99
3
0.
9
9
4
0.
98
5
0.
99
1
0.
98
5
0.
98
5
0.
99
0
0.
98
4
0.
98
7
0.
99
0
0.
99
1
Cr
#
66
10
11
62
70
69
67 55 70
24
15
66
74
53
60
46 58
80
65 28
Mg
#
60
78
74
64
58
55
59 63 48
67
78
57
49
56
63
64 59
61
55 75
Table 3:
Representative microprobe analyses of
Cr-spinels from the Czor
styn Unit (in wt. %). Formula
is based on 3 cations.
*Fe
2
O
3
calculated from stoichiometry. Cr#
= Cr/(Cr+Al); Mg# = Mg/(Mg+
Fe
2+
).
tions can be interpreted as derived
from at least two separate sources. The
first source supplied the detritic mate-
rial earlier, as it is identical with the
source of Jurassic clastics in the
Czorsztyn Unit. The source most like-
ly represented magmatic and meta-
morphic rocks forming the Czorsztyn
elevation. The heavy mineral assem-
blage derived from this source is dom-
inated by garnet, with decreasing
amounts of zircon, rutile and tourma-
line (Aubrecht 1993, 2001). Composi-
tion of the detrital garnets is the same
as of those presented in this paper (cf.
Aubrecht & Méres 2001).
The second source is similar to the
source of exotic clastics in the Albian
of the Klape Unit and the Tatric and
Fatric units of the Central Western
Carpathians (Jablonský 1978, 1986;
Mišík et al. 1980, 1981; Jablonský et
al. 2001). The heavy mineral assem-
blages derived from this source are
characterized by strong prevalence of
spinels (mainly Cr-spinels) and zir-
con, followed by tourmaline and
rutile. The sources of both assem-
blages are the subjects of long-lasting
debates. The solution of this problem
would provide answers to the crucial
questions which remain in the Meso-
zoic paleogeography of the Western
Carpathians.
Source of the garnets
Composition of the detrital garnets
shows that they were derived from pa-
rental rocks such as UHP eclogites or
garnet peridotites, HP eclogites and
HP mafic granulites, felsic and inter-
mediate granulites, gneisses and am-
phibolites metamorphosed under the
transitional, granulite to amphibolite
facies conditions and gneisses and am-
phibolites metamorphosed under am-
phibolite facies conditions. These rock
types are typical of the polymetamor-
phosed complexes, in which the first
metamorphic event took place under
HP/UHP conditions. The metamor-
phic complex was then exhumed and
retrogressively recrystallized under
the granulite and amphibolite facies
conditions.
Such
metamorphosed
complexes are known in the European
Variscides (e.g. Dora Maira Massif of
the Western Alps, Bohemian Massif,
476
AUBRECHT, MÉRES, SÝKORA and MIKUŠ
Massif Central, leptyno-amphibolite complex in the Western
Carpathians) and in the Western Gneiss Region of the Norwe-
gian Caledonides.
The detrital garnets presented in this paper have predomi-
nantly specific composition (almandine-pyrope and grossular-
pyrope-almandine) which corresponds well with the detrital
garnets from the Jurassic sandy limestones of the Czorsztyn
Unit, but they were also found in the Jurassic limestones of the
Klape Klippe and in the Manín Unit of the Pieniny Klippen
Belt (Aubrecht & Méres 2000). Except for this zone, almand-
Fig. 9. Al
2
O
3
vs. TiO
2
compositional relationships of the analysed
spinel grains. For comparison, Cr-spinels from (grey fields with dot-
and dashed line) the Mesozoic ultramafic bodies of the Western Car-
pathians (Meliata Unit) are plotted (Mikuš & Spišiak 2007). The
spinels are compared with compositional fields of spinel from volcanic
rocks and mantle peridotites (according to Kamenetsky et al. 2001).
a – peridotite spinels; b – volcanic spinels (MORB = mid-oceanic
ridge basalts, SSZ peridotite = supra-subduction zone peridotite).
Fig. 10. Mg/(Mg + Fe
2+
) vs. Cr/(Cr + Al) diagram of the analysed
spinels (after Dick & Bullen 1984).
ine-pyrope garnets are also characteristic for other zones of the
Western Carpathian externides. They were reported from the
Cretaceous to Paleogene sediments of the Carpathian Flysch
Zone (Otava et al. 1997, 1998; Salata 2004; Oszczypko &
Salata 2005; Grzebyk & Leszczyński 2006). The data from the
Flysch Zone are not restricted solely to garnets from heavy
mineral assemblages but exotic granulitic pebbles (one of the
potential source rocks) were reported from the Silesian Unit
by Wieser (1985). Almandine-pyrope garnets are lacking in
the crystalline rocks of the Western Carpathian internides
Fig. 11. Nomenclature and composition of spinels based on the
classification of Deer et al. (1992). The studied spinels are com-
pared with spinels of the Meliata Unit and adjacent tectonic units
(Klape and Manín Units). The compared compositional fields are
according to Mikuš (2005).
477
DETRITAL GARNETS AND SPINELS FROM THE ALBIAN SEDIMENTS (PIENINY KLIPPEN BELT)
(Aubrecht & Méres 2000). Very similar pyrope-rich garnets
are known from the metamorphic rocks (garnet peridotites,
garnet pyroxenites, kyanite eclogites and granulites) of the
Bohemian Massif (Scharbert & Carswell 1983; O’Brien &
Vrána 1995; Medaris et al. 1995a,b, 1998, 2005, 2006a,b;
O’Brien et al. 1997; Nakamura et al. 2004). Because of the
presence of granulite-derived detritus, the crustal segments of
the Western Carpathian externides, including the Pieniny
Klippen Belt, were interpreted as being derived from the
Moldanubian Zone of the Bohemian Massif (Aubrecht &
Méres 1999, 2000). However, almandine-pyrope to garnets
very rich in pyrope contents are also abundant in the Batho-
nian-Lower Callovian sands in the Cracow-Wieluń Upland
which is an epi-Hercynian platform and was relatively stable
during the Mesozoic (Aubrecht et al. 2007). These occurrenc-
es are too distant from the Moldanubian Zone. Apart from this
zone, there are only two other known proximal occurrences of
granulites and eclogites – the Góry Sowie Block and the
Śnieźnik area complex in the Western Sudetes (Smulikowski
1967; Oberc 1972; Kryza et al. 1996; O’Brien et al. 1997).
They are, however, too small to be a regionally important
source of clastic material. Exotic, pyrope-almandinic garnets
were also reported from the Carboniferous of the Moravo-
Silesian Culm Basin (Otava & Sulovský 1998; Otava et al.
2000; Hartley & Otava 2001; Čopjaková et al. 2001, 2005).
Some granulitic pebbles were also found in the Carboniferous
sediments of the Upper Silesia Coal Basin (Paszkowski et al.
1995). In the Carboniferous clastics of the Moravo-Silesian
Zone, the authors invariably derive the clastic material from
the Moldanubian Zone of the Bohemian Massif (Paszkowski
et al. 1995; Hartley & Otava 2001).
Source of the spinels
The presence and overall dominance of spinels in the heavy
mineral assemblage of the Chmielowa Formation is surpris-
ing. They most likely represent clastics from a source which
was different from the garnet source, although small part of
the spinels might also be derived from the same metamorphic
complex as the high-pyrope garnets, because Cr and Al
spinels usually occur also in the metaperidotites, eclogites and
polymetamorphosed equivalents of the granulite facies. How-
ever, such spinels would appear already in the Jurassic or
Lower Cretaceous detritus-bearing sediments of the Czorsztyn
units (Middle Jurassic and Valanginian crinoidal limestones)
which is not the case (Łoziński 1959; Aubrecht 1993, 2001).
Similarly unlikely is the possibility that originally rare, but re-
sistant spinels were enriched by reworking and dissolution in
the condensed facies overlying the paleokarst surface. The
previous inherited assemblage, also containing less stable
minerals, such as garnet and kyanite, bears no signs of deple-
tion. Therefore, most of the spinels were probably derived
from the source which could have been identical to the source
of the Albian exotics in the Klape Unit of the Pieniny Klippen
Belt and in the Tatric and Fatric units of the Central Western
Carpathians. However, this source is unknown to date and
many publications were already dedicated to this topic. The
first research concerning West Carpathian exotics was made
by Matějka & Andrusov (1931), Zoubek (1931) and Andrusov
(1938) who investigated the “Upohlav” conglomerates in the
Pieniny Klippen Belt. Their source was interpreted as an exot-
ic Pieniny Ridge (Andrusov 1938, 1945) which was later re-
named by Birkenmajer (1988) as the Andrusov Ridge.
According to Birkenmajer (1977, 1988), the Andrusov Ridge
was placed south of the Kysuca-Pieniny Basin (passing to an
oceanic crust) and north of the Central Western Carpathians.
According to Marschalko (1986), the transport direction of the
exotics in the Klape Unit was from south and south east. That
would indicate position of the Klape Unit north of the Andrusov
Ridge. This opinion was challenged by Birkenmajer (1988)
who placed this unit south of the ridge. From the beginning,
the researchers considered that all the exotic conglomerates
were Senonian, but later works brought data about the earlier,
Albian onset of the exotic sedimentation (e.g. Began et al.
1965; Samuel et al. 1972). The first Cr-rich spinels were even
reported from the Barremian-Aptian limestone pebbles from
the exotic conglomerates (Mišík et al. 1980), the same was re-
ported from the Eastern Alps (Wagreich et al. 1995). Albian-
Cenomanian exotic flysch (including exotic conglomerates) is
also widespread in the Tatric and Fatric units of the Central
Western Carpathians where it is named the Poruba Formation
(Jablonský 1978, 1986). The transport directions in this unit,
however, largely differ from those in the Klape Unit
(Jablonský 1986). The data in the Tatric units are largely scat-
tered but generally trough-parallel transport dominated, with
some lateral transport directions coming from the south (in
Nízke Tatry Mts). In the Fatric units (Krížna Nappe) there
were both, southern and northern sources indicated by the
measurements. Because of these facts, Mišík et al. (1980)
suggested the presence of two additional exotic sources, the
Ultratatric and the Ultrakrížna ridges, which made the paleo-
geographical situation quite complicated. Even earlier occur-
rences of exotic ophiolitic detritus (Cr-rich spinels) were
indicated in the Hauterivian sandstone turbidites in the Fatric
and Hronic (Choč Nappe) units (Jablonský 1992). Further to
the south, Hauterivian to Albian flysches with Cr-rich spinels
occur in the northern part of the Transdanubian Central Range
(Árgyelán 1992, 1996; Császár & Árgyelán 1994), where the
first Cr-rich spinels appeared already in the Upper Jurassic
limestones of the Gerecse Mountains (Árgyelán & Császár
1998). This ophiolitic detritus was invariably derived from the
suture of the Meliata Ocean which was open in the Middle
Triassic and closed in the Late Jurassic. Even in the Middle
Jurassic matrix of the Meliatic subduction melange, chrome
spinels are present, although in minor amounts (Mock et al.
1998). The Meliata suture zone is situated south of the Central
Western Carpathians and is considered to be a boundary be-
tween them and the Inner Western Carpathians further to the
south. The Andrusov Ridge was supposed to be situated north
of the Central Western Carpathians and was considered to be
an accretionary wedge formed by subduction of the younger,
Penninic-Vahic Ocean (e.g. Mahe 1981, 1989; Birkenmajer
1988). The resedimented ophiolitic remnants in the Pieniny
Klippen Belt were then considered to represent another impor-
tant suture zone in the Western Carpathians. However, the sit-
uation with the Andrusov Ridge is more complex. Pebbles of
basaltic volcanics of the Late Jurassic—Early Cretaceous K-Ar
age (Rybár & Kantor 1978; Birkenmajer & Pécskay 2000)
478
AUBRECHT, MÉRES, SÝKORA and MIKUŠ
would fit the Penninic ophiolites. Some exotics were apparently
derived from the Carpathian Foreland, for example Namurian
black coal (Havlena 1956; Šilar 1956) or non-metamorphosed
Devonian limestone (Tomaś et al. 2004). Along with the
above mentioned rock types, there are many exotics which
seem to be derived from more southern zones representing the
Inner Western Carpathians and even Dinarides. There are peb-
bles from blocks of southern types of Triassic, such as the
Wetterstein-type platform limestones typical for the Silicic
units; exotic granitic pebbles (the so-called Upohlav-type) are
the most similar to those of A-type granites, as in the Turčok or
Velence Massif (Uher & Marschalko 1993; Uher & Pushkarev
1994; Uher et al. 1994; Uher & Broska 1996). The Devonian
limestone pebbles mentioned above might be alternatively de-
rived from a more southern source, such as the Transdanubian
Central Range. Very characteristic are deep-water to oceanic
Triassic sediments indicating their relationship with the Meliata
Ocean (Mišík et al. 1977; Birkenmajer et al. 1990). The Triassic
deep-sea deposits are even older (Lower Anisian) than those
found in the Meliata Unit. Moreover, radiometric datings of
some glaucophanite pebbles showed Jurassic age of metamor-
phism which is in accordance with the closure of the Meliata
Ocean (Dal Piaz et al. 1995). Meliata-like elements in the ex-
otic conglomerates led to speculations about proximity of the
Meliata and Oravic domains (e.g. Mišík 1978; Mišík & Sýkora
1981), although later some authors favoured an alternative ex-
planation about two different Triassic troughs south and north
of the Central Western Carpathians (Birkenmajer et al. 1990).
In the Eastern Alps, where the situation of the exotics is very
similar to the Western Carpathians, there is also a long lasting
debate about the northern (Penninic) and southern (Meliata—
Vardar) sources of ophiolite detritus in Cretaceous sediments
(e.g. Decker et al. 1987; Pober & Faupl 1988; Faupl & Pober
1991; Faupl & Wagreich 1992; Wagreich et al. 1995; Eynatten
& Gaupp 1999). An attempt to unify both sources led Plašienka
(1995, 1996) to a radical opinion that the Klape Unit belongs
to the Fatric domain and its exotic flysches represent just
a proximal part of the Poruba Formation turbiditic fan. There
are, however, many counterarguments against this opinion
(Mišík 1996). The data presented in this paper also contradict
this theory.
New paleogeographical model of the Pieniny Klippen Belt
In spite of the still unknown source of the ophiolite detri-
tus, in most reconstructions it is placed much further south
than the presumed sedimentary area of the Czorsztyn Unit.
The reconstruction of the Oravic (Pienidic) domain made by
Birkenmajer (1977) was accepted with small modifications up
to the present time. However, in the light of the presence of
the Cr-rich spinels in the Albian sediments of the Czorsztyn
Unit, this reconstruction is problematic. According to this
concept, the Czorsztyn Unit sedimented on an isolated swell
which was separated in the Cretaceous from the Carpathian in-
ternides by the so-called Kysuca-Pieniny Trough, which in lat-
er interpretations of Birkenmajer (1988) was considered one of
the branches of the Penninic Ocean. In the Albian, the input of
exotics (including ophiolite detritus) was concentrated only in
the more southern units (in the sense of previous reconstruc-
tions), such as the Klape Unit, Tatric and Fatric units (see
above). Moreover, the first sandstone turbidites also appeared
in the Upper Albian of the Manín Unit (Marschalko & Rakús
1997). However from the Oravic units they were known only
from the Coniacian-Santonian Sromowce Formation of the
Kysuca-Pieniny Unit. Although there is a rare occurrence of
Albian flysch (Trawne Member) mentioned from the Kysuca
Unit by Birkenmajer (1987) it is not clear whether it bears
some exotics. In the Turonian sandstone flysch (Snežnica For-
mation), there is still lack of Cr-rich spinels (Łoziński 1959;
Aubrecht – unpublished data). This is the reason why the lat-
est Aptian appearance of ophiolitic detritus in the Czorsztyn
Unit is so surprising. The question is: How can this detritus,
derived from the south, reach an isolated elevation surrounded
by deep troughs? The Czorsztyn Unit in the Cretaceous was
still situated on an elevated area, as indicated by Aubrecht et
al. (2006). However, the presence of exotic ophiolitic detritus
indicates that it was not an isolated elevation but this sedimen-
tary area must have been adjacent to the exotic source.
For these reasons, we propose an alternative paleogeograph-
ical model of the Pieniny Klippen Belt evolution (Figs. 12,
13). Middle Jurassic Penninic rifting caused detachment of the
Oravic segment from its position in continuation of the Molda-
nubian Zone of the Bohemian Massif. The SW-NE orientation
of the initial rifting corresponds to many paleogeographical re-
constructions (see discussion in Aubrecht & Túnyi 2001).
Derivation from the Moldanubian Zone is based on the garnet
compositions presented by Aubrecht & Méres (2000) and in
this paper. The Oravic segment was originally situated in lat-
eral continuation of the Central and Inner West Carpathian
segments (Michalík 1994). In an earlier period the Triassic
Meliata Ocean was situated south of both segments. This
ocean was closed in the Late Jurassic when the crustal seg-
ments derived from the North-European Platform collided
with South-Alpine/Dinaridic segments. Remnants of the
ocean were arranged in subduction melange along the Meliata
suture zone. During the Cretaceous, the amalgamated blocks
were further rotated clockwise to the final NW-SE orientation
(for the pre-Paleogene orientation of the Central Western
Carpathians, see Túnyi & Márton 2002 and Csontos & Vörös
2004). The rotation caused detachment of the Oravic segment
from its lateral position and its relative lateral shift along the
northern margin of the Central Western Carpathians. The
Meliatic melange was then secondarily placed in the zone
between the Oravic segment and the Central Western Car-
pathians where it formed an elevated ridge (the exotic Andrusov
Ridge) which was the source of exotic pebbles and ophiolitic
detritus, feeding simultaneously the Klape, Tatric and Fatric
units on the SW and the Oravic units on the NE. Such arrange-
ment of the exotic source fits well with the conclusions of
Marschalko (1986) who suggested that the exotic ridge repre-
sented a long-lasting elevation formed in a strike-slip zone
rather than compressional wedge which would be destroyed in
a short time. Early presence of the ophiolitic detritus in the
Czorsztyn Unit indicates that it was closer to the exotic ridge
and no depression occurred between them, which would pre-
vent transport of this material to the Czorsztyn sedimentary
area. The ophiolitic material (dominated by spinels) was
mixed with the material from the still emerged Czorsztyn
479
DETRITAL GARNETS AND SPINELS FROM THE ALBIAN SEDIMENTS (PIENINY KLIPPEN BELT)
Fig. 13. New proposed paleogeographical reconstruction of the Pieniny Klippen Belt units in the Albian.
Fig. 12. New proposed paleogeographical scheme of the Pieniny Klippen Belt (Middle Jurassic to Early Cretaceous) evolution in the con-
text of the other Alpine-Carpathian units (see the comments in the text). Abbreviations: L. Austroalpine = Lower Austroalpine, U. Aus-
troalpine = Upper Austroalpine, CWC = Central Western Carpathians, IWC = Inner Western Carpathians.
480
AUBRECHT, MÉRES, SÝKORA and MIKUŠ
Swell (garnet-dominated heavy mineral assemblages). The el-
evation difference between the Czorsztyn and the exotic An-
drusov Ridge was not big and only relatively fine detritus was
transported to the Czorsztyn sedimentary area (both, Jurassic
and Cretaceous clastics in the Czorsztyn Unit are of the same
size – maximum 2—3 cm pebbles). On the contrary, the exot-
ic pebbles in the Klape and Tatric units reach size from some
decimeters to meters.
This paleogeographical reconstruction requires radical
change in the interpretation of the Oravic zonation (Fig. 13).
In the new interpretation we keep the original arrangement of
Birkenmajer (1977) (with slight modification of Wierzbowski
et al. 2004) but the entire orientation of the Oravic segment
should be reversed by 180°. This means that the Kysuca-Pien-
iny sedimentary area would continue to the Magura Ocean
and no trough existed between the Central Western Car-
pathians and the Czorsztyn Swell. The northward arrangement
of the Oravic units is more logical as the SE-NW oriented ex-
tension (rifting) usually causes crustal block tilting in which
the riftward side is steeper and the landward side dips more
gently (the reconstruction of Birkenmajer 1977 shows the op-
posite). Therefore, there was much larger space on the land-
ward (generally northern) side to arrange all the gradually
deepening Oravic units.
Conclusions
1. Heavy mineral analysis of the Upper Aptian-Albian sedi-
ments from the Chmielowa Formation of the Czorsztyn Unit
of the Pieniny Klippen Belt shows a dominance of spinels and
garnets over zircon, rutile and tourmaline.
2. The composition of majority of the detrital garnets shows
that they were derived from primary HP/UHP parental rocks
which were recrystallized under granulite and amphibolite fa-
cies conditions. Such garnets are of exotic origin but the same
were found in the Jurassic clastics of the Czorsztyn Unit.
Therefore, garnets despite being exotic, are considered to be
derived from the presently non-existing crystalline rocks of
the Oravic crustal segment.
3. Detrital spinels are a new element in the Aptian/Albian
Oravic paleogeography. They were most likely derived from
the same exotic sources as clastics of the Klape, Tatric and
Fatric units. The presence of ophiolitic detritus in the sedi-
ments which sedimented on the Czorsztyn Elevation infer that
this elevation was not isolated from the exotic source by deep-
er troughs but it was in close vicinity to it. A small part of the
spinels might also be derived from the same metamorphic
complex as the high-pyrope garnets.
4. A new paleogeographical model for the Pieniny Klippen
Belt is proposed: The Oravic segment was derived from the
Moldanubian Zone of the Bohemian Massif by the Middle Ju-
rassic rifting. The rifting caused block tilting where most of
the Oravic units were arranged north of the Czorsztyn Swell,
dipping to the Magura (Penninic) Ocean. The Oravic segment
was situated in the lateral continuation of the Central and In-
ner Western Carpathians. Later clockwise rotation caused de-
tachment of the Oravic segment, which was laterally shifted in
front of the Central Western Carpathians, together with rem-
nants of the Meliata suture zone. The latter served as a source
of the exotics to the Klape, Tatric, Fatric and Oravic units.
Acknowledgments: The authors wish to express their thanks
to the reviewers doc. Pavel Uher (Comenius University, Slo-
vakia), prof. Peter Faupl (Vienna University, Austria), as well
as to the GC responsible editor prof. Dušan Plašienka for their
thorough reviews, which considerably improved the quality of
this paper. This work was financially supported by the Slovak
Research and Development Agency under the contracts
No. APVV-0571-06, 0465-06, 0279-07 and VEGA grant
agency by Grants No. 1/4035/07 and 1/4039/07.
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