GEOLOGICA CARPATHICA
, FEBRUARY 2019, 70, 1, 15–34
doi: 10.2478/geoca-2019-0002
www.geologicacarpathica.com
Provenance of synorogenic deposits of the Upper
Cretaceous–Lower Palaeogene Jarmuta–Proč Formation
(Pieniny Klippen Belt, Western Carpathians)
JOZEF MADZIN
1,
, DUŠAN PLAŠIENKA
2
and ŠTEFAN MÉRES
3
1
Earth Science Institute, Slovak Academy of Sciences, Ďumbierska 1, 974 01 Banská Bystrica, Slovakia;
jozef.madzin@savba.sk
2
Department of Geology and Palaeontology, Faculty of Natural Sciences, Comenius University, Mlynská dolina, Ilkovičova 6,
842 15 Bratislava, Slovakia; dusan.plasienka@uniba.sk
3
Department of Geochemistry, Faculty of Natural Sciences, Comenius University, Mlynská dolina, Ilkovičova 6, 842 15 Bratislava, Slovakia;
stefan.meres@uniba.sk
(Manuscript received July 12, 2018; accepted in revised form January 11, 2019)
Abstract: The Pieniny Klippen Belt contains thickening and coarsening upwards synorogenic sedimentary successions
witnessing the collision of the Oravic ribbon continent with the Central Carpathian orogenic wedge after the closure of
the Vahic Ocean in the Late Cretaceous to Early Palaeogene. The sedimentary record of this event is represented by
flysch/wildflysch deposits of the Maastrichtian–Lower/Middle Eocene Jarmuta–Proč Formation. We present results of
the provenance study of these deposits, based on the framework petrography, heavy mineral analysis and mineral
chemistry. Turbiditic sandstones were classified as quarzolithic to lithic arenites. Lithic fragments are predominantly
composed of carbonate rocks and low- to medium-grade metamorphic and occasional mafic volcanic rocks. The heavy
mineral association is composed of both first-cycle derived and recycled ultrastable ZTR, garnets and Cr-spinels.
The chemistry of the detrital tourmalines and garnets suggests a derivation from various low- to medium-grade metamorphic
rocks. High-pyrope garnets, observed in the eastern part of the PKB, which were derived from high-grade granulites and
eclogites, represent probably lower crustal complexes exhumed during rifting of the Vahic Ocean. The Cr-spinels show
a mixed harzburgitic and lherzolitic provenance. The harzburgitic Cr-spinels might have been recycled from older exotic
conglomerates of the Klape Flysch, thereby representing ophiolitic detritus of the Meliata Ocean. The lherzolitic
Cr-spinels might represent a new contribution of ophiolitic detritus delivered from the exhumed subcontinental mantle
forming the Vahic oceanic floor.
Keywords: Western Carpathians, Pieniny Klippen Belt, synorogenic deposits, petrography, heavy mineral analysis,
mineral chemistry, provenance.
Introduction
The Pieniny Klippen Belt (PKB) is one of the structurally
most complicated zone of the Western Carpathians (WC),
separating the External Western Carpathians (EWC; Tertiary
accretionary complex — Flysch Belt) from the Central
Western Carpathians (CWC; Cretaceous Austroalpine–Slovako-
carpathian basement–cover thrust stack) (e.g., Plašienka et al.
1997; Plašienka 1999, 2018a; Froitzheim et al. 2008).
The PKB includes Jurassic to Palaeogene sediments
detached from its completely subducted basement of unknown
character. Its complex polyphase structural deformation domi-
nated by the Palaeocene to Eocene nappe thrusting resulted
in the superposition and juxtaposition of numerous litho-
logically and palaeogeographically distinct tectonic units (see
e.g., Birkenmajer 1977, 1986; Mišík 1997; Jurewicz 2005;
Plašienka & Mikuš 2010; Plašienka 2012a). Later, during
the Early and Middle Miocene, the PKB experienced further
strong deformation including out-of-sequence thrusting, trans-
pression, transtension, backthrusting, and block rotations,
which obliterated original fold-and-thrust structures resulting
in its complicated spectacular “klippen” structure (e.g.,
Ratschbacher et al. 1993; Kováč & Hók 1996; Plašienka &
Jurewicz 2006; Plašienka 2012b, 2018b). Therefore, the PKB
is often characterized as a peculiar block-in-matrix structure
or mélange formed by isolated rigid blocks “klippen” com-
posed of competent Middle Jurassic to Lower Cretaceous car-
bonates surrounded by a soft matrix of the “klippen mantle”
consisting of Lower Jurassic and Upper Cretaceous to
Palaeogene shales, marls and flysch formations (e.g.,
Birkenmajer 1977; Plašienka & Mikuš 2010).
The main tectonic units of the PKB s.s., were derived from
an independent palaeogeographic domain known as the Oravic
domain or Oravicum (Maheľ 1986). It is thought that
the Oravic domain represents the continental crustal fragment
in the Middle Penninic position (analogous to the Briançonnais
microcontinent) surrounded by North Penninic (Valais–
Rhenodanubian–Magura) (e.g., Schmid et al. 2008) and South
Penninic (Ligurian–Piemont–Vahic–Iňačovce) oceanic domains
as a continuation of the Alpine Atlantic oceanic tract from
the Alps to the Carpathians (Plašienka 2003, 2012a; Froitzheim
et al. 2008; Plašienka & Soták 2015). Consequently, the sup-
posed suture-like structure of the PKB, although ophiolites do
not participate in its recent surface structure, is related to
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MADZIN, PLAŠIENKA and MÉRES
GEOLOGICA CARPATHICA
, 2019, 70, 1, 15–34
the collision of the Oravic ribbon continent with the frontal
parts of the CWC orogenic wedge after the closure and sub-
duction of the Vahic oceanic domain (Plašienka 2012a).
Whether, and to what extent, the Vahic (South Penninic) and
likewise the Magura (North Penninic) basins, were floored by
an oceanic crust is still a matter of debates and controversy
(e.g., Winkler & Ślączka 1992, 1994; Rakús & Hók 2005;
Aubrecht et al. 2009; Oszczypko et al. 2015).
The sedimentary record of the contractional tectonic pro-
cesses is represented by a turbiditic sequence of the Turonian
Snežnica Fm. and the Coniacian–Santonian Sromowce Fm.
including bodies of exotic conglomerates (Pieniny Unit;
Plašienka 2012a and references therein), and the Upper
Cretaceous–Lower/Middle Eocene synorogenic flysch or
wildflysch Jarmuta–Proč Formation consisting of turbiditic
sandstones with huge olistostromatic bodies (Gregorianka
Breccia Member of the Sub-Pieniny Unit and Milpoš Breccia
Member of the Šariš Unit) (Plašienka & Mikuš 2010; Plašienka
2012a; Plašienka et al. 2012).
Rocks referable to the Jarmuta Fm. or to the Jarmuta–Proč
Fm. have been known since the 1930s (e.g., Horwitz 1932).
However, data about its sedimentology, petrography (Leško
1960; Ďurkovič 1972), heavy mineral composition (Starobová
1962; Łoziński 1966; Winkler & Ślączka 1992, 1994), and
mineral chemistry (Salata 2002, 2004; Oszczypko & Salata
2005; Bónová et al. 2018) are contradictory in some aspects
(e.g., Birkenmajer 1977, 1986; Nemčok et al. 1989; Plašienka
& Mikuš 2010). On the other hand, the cited works suggest
the crucial importance of the synorogenic sediments for under-
standing the early development of the PKB (Plašienka &
Mikuš 2010; Plašienka et al. 2012).
The aim of this paper is to contribute to the provenance
analysis of the Jarmuta–Proč Fm. based on the framework
petrography, heavy mineral analysis and mineral chemistry of
detrital tourmalines, garnets and Cr-spinels.
Geological settings
Most of the samples were collected from the Pieniny, Šariš
and Beňatina sectors (according to the classical division by
Scheibner 1967; Vass 1988; Mišík 1997) of the PKP in eastern
Slovakia (Fig. 1). Recently, a new model for the structure and
development of the PKB has been demonstrated from this area
(Plašienka & Mikuš 2010; Plašienka 2012b; Plašienka et al.
2012). Three principal superposed Oravic tectonic units of
the PKB have been distinguished. These are the Šariš (formerly
named Fakľovka Unit by Plašienka & Mikuš 2010), the Sub-
Pieniny and Pieniny thrust sheets from bottom to top. All of
the Oravic units are characterized by varied Jurassic to Upper
Cretaceous–Palaeogene coarsening- and thickening-upwards
synorogenic sedimentary successions deposited in the front of
the advancing thrust sheets (Fig. 2).
The Šariš unit (for more details see Plašienka & Mikuš
2010; Plašienka 2012 a, b; Plašienka et al. 2012) occurs in
the lowermost structural position and includes a strongly
dismembered basinal Jurassic to Lower/Middle Eocene sedi-
mentary succession. The top of the Šariš unit is composed of
a hundred metres of sandstone-dominated flysch or wildflysch
sequence of the latest Cretaceous to Lower/Middle Eocene
Jarmuta–Proč Fm. (JPF) with bodies of mass-transport depo-
sits including numerous huge olistoliths (Milpoš Breccia
Member; Plašienka & Mikuš 2010). A variegated clastic mate-
rial and olistoliths were mainly derived from sedimentary suc-
cessions of the overriding Sub-Pieniny and Pieniny nappes
(Plašienka & Mikuš 2010).
The Sub-Pieniny Unit exhibits an intricate structure inclu-
ding the typical shallow-marine Middle Jurassic to Lower
Cretaceous Czorsztyn succession, as well as the slope-derived
“transitional” Niedzica/Czertezik successions (e.g., Ožvoldová
et al. 2000; Wierzbowski et al. 2004). The sedimentary succes-
sion of the Sub-Pieniny Unit is terminated by comparatively
thin calcareous sandstones of the JPF (Maastrichtian–
Danian?), which includes mass-transport deposits in the upper
parts (Gregorianka Breccia Member; Nemčok et al. 1989;
redefined by Plašienka & Mikuš 2010). The Gregorianka
Breccia Member is composed of monotonous detrital material
derived evidently from the overriding Pieniny nappe (Plašienka
et al. 2012).
The Pieniny Unit occurs in the most internal and the upper-
most structural position of the PKB tectonic entity as a late-
rally continuous thrust sheet (Plašienka 2012b). It comprises
mainly a deep-water Jurassic to Upper Cretaceous succession
terminated by a coarsening- and thickening-upwards syn-
orogenic turbiditic sequence of the Turonian Snežnica Fm.
and the Coniacian–Santonian Sromowce Fm. (Plašienka
2012a).
Methods
Framework petrography
The framework petrography was carried out on 72 sand-
stone samples of the JPF taken from 15 geographically distri-
buted localities throughout the PKB (Fig. 1, Supplementary
Table S1). Petrographic features of the sandstones including
mineral constituents, grain size, sorting, and roundness were
observed by using a polarizing microscope. The samples were
selected from medium to coarse-grained sandstones in order to
get the maximum source rock information. In order to elimi-
nate different grain size issues (Ingersoll et al. 1984), analyses
from the individual grain-sizes were plotted separately in
the classification diagrams (Figs. 3, 4). At least 300 grains in
each thin section were counted. The point-counting method
followed the approach of von Eynatten & Gaupp (1999). This
approach is more useful in synorogenic coarse-grained sedi-
ments than the classical Gazzi–Dickinson method (the GD
method as described by Ingersoll et al. 1984), where minerals
or crystals ˃ 63 μm in polycrystalline fragments are counted
separately. For example, following the GD method, a signifi-
cant amount of polycrystalline mica–quartz aggregates would
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, 2019, 70, 1, 15–34
be assigned to the monocrystalline quartz category, thereby
a metamorphic origin of these clasts may be overlooked.
Because of the high amount of carbonate clasts (L
carb
=
limestones + dolomites), they were attributed to the category
of lithic fragments (L) together with other non-carbonate
lithic fragments (L
s
), which is not usual in classic provenance
studies (Dickinson & Suzcek 1979; Dickinson 1985).
However, carbonate clasts were eroded and transported
through the same processes as any clastic material and over-
looking and non-counting of the carbonate clasts would have
led to a partly incorrect classification of the analysed rocks,
and therefore, to a biased provenance interpretation. Carbonate
allochems, such as intrabasinal carbonate bioclasts, following
discrimination criteria proposed by Zuffa (1985) were not
counted.
Heavy mineral analysis
Ten samples of medium- to coarse-grained sandstones/fine-
grained conglomerates of the JPF and Milpoš Breccia Mb.
(MB) were selected for the heavy mineral analysis (Table 1).
The separation and preparation of heavy minerals followed
the standard procedures described by Mange & Mauer (1992).
The 80–250 µm fraction was examined under both a pola-
rizing and a binocular microscope. At least 200 grains were
counted using the ribbon counting method (Galehouse 1971)
and are shown as number percentages (Table 2).
Mineral chemistry
Detrital tourmalines, garnets and Cr-spinels from the selec-
ted sandstone samples (Table 1) were hand-picked, mounted
in epoxy resin, polished and coated with carbon for electron
microprobe analysis.
The chemical composition of the separated detrital minerals
were analysed using a CAMECA SX-100 electron microprobe
at State Geological Institute of Dionýz Štúr in Bratislava.
The analytical conditions were a 15 kV accelerating voltage
and a 20 nA beam current with peak counting time of 20 s and
a beam diameter of 2–10 μm. Raw counts were corrected
using a PAP matrix correction (Pouchou & Pichoir 1985).
To measure various elements the following natural and syn-
thetic standards were used: wollastonite (SiK
α
, CaK
α
), TiO
2
(TiK
α
), Al
2
O
3
(AlK
α
), pure Cr (CrK
α
), pure V (VK
α
), fayalite
(FeK
α
), rhodonite (MnK
α
), forsterite (MgK
α
), willemite
(ZnK
α
), pure Ni (NiK
α
), albite (NaK
α
), orthoclase (KK
α
),
BaF2 (FK
α
) and NaCl (ClK
α
). Lower detection limits of
the measured elements varied between 0.01 and 0.05 wt. %;
V, Cr, Mn, Zn, Ni, F, and Cl were also below their respective
detection limits.
Overall 45 analyses of detrital tourmalines from five JPF
and two MB samples were performed (Suppl. Table S2).
Detrital tourmalines were analysed by using one to three
single-spots located over centres and/or along rims of
grains. The crystallo-chemical formulae of tourmaline were
Fig. 1. A –– Location of the study areas in the frame of the Alpine–Carpathian–Pannonian–Dinaridic tectonic system; B, C — tectonic sketch
maps with location of the sampled sites (modified after Kováč et al. 1998; Bezák et al. 2004).
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GEOLOGICA CARPATHICA
, 2019, 70, 1, 15–34
calculated on the basis of 15 Y + Z + T cations,
W
O
2−
was
obtained from the charge-balanced formula, OH was calcu-
lated as OH = 4 − Cl −
W
O apfu, B = 3 apfu.
Overall 35 analyses of detrital garnets separated from seven
localities of the JPF and MB were performed (Suppl.
Table S3). The crystallo-chemical formula of garnet was nor-
malized to 12 oxygens and conversion of iron valence (Fe
3+
and Fe
2+
) according to ideal stoichiometry.
Chemical compositions of 15 detrital Cr-spinels from six
localities of the JPF and MB were examined (Suppl. Table S4).
Analyses of detrital Cr-spinels were calculated on the basis of
3 cations. Fe
2+
and Fe
3+
in spinel were allocated according to
the ideal stoichiometry.
Results
Framework petrography
The JPF consist mainly of grey, grey brown, and grey blue
fine- to coarse- and very coarse-grained sandstones/fine-
grained conglomerates with occasional intercalations of cal-
careous grey to grey brown mudstones. It is apparent that
the detrital material of the sandstones and their coarse-grained
equivalents, the Milpoš Breccia Member, is the same.
Texturally, the studied sandstones can be regarded as
sub-mature, since they are moderately sorted, composed
mostly of angular, sub-angular to sub-rounded grains (Fig. 5).
Compositionally, the sandstones are immature,
because of the high content of lithic, mostly car-
bonate grains. The matrix of the sandstones
occurs very rarely and the sandstones are
cemented mostly by carbonate cement. According
to the classification scheme introduced by
Pettijohn et al. (1972), the analysed sandstones
are predominantly lithic arenites, less sub-lithic
are nites and one sample is characterized as sub-
arcosic arenite (Fig. 3A). Based on the classi fi-
cation diagram proposed by Garzanti (2016)
the stu died sandstones are classified predomi-
nantly as litho–quartzitic, feldspatho–litho– quar-
tzitic to quartzo–lithic sandstones and one sample
as feldspatho–quartzitic sandstone (Fig. 3B).
Medium-grained sandstones plot in the classifi-
cation diagrams closer to the Q pole than their
coarse-grained equivalents.
The main components of the sandstones are
quartz (Q) and lithic grains (L).
Quartz (Q
t
) is represented by both monocrystal-
line and polycrystalline forms. The monocrystal-
line quartz (Q
m
) is a ubiquitous component of
the analysed sandstones. The polycrystalline
quartz (Q
p
) consists of either a fine-grained chert
and/or a mica-quartz aggregate mostly of a meta-
morphic origin.
Feldspar contents (F) are usually low (on ave-
rage about 3 %) (Figs. 3, 4; Suppl. Table S1).
K-feldspars outweigh plagioclases and are repre-
sented by orthoclase, with occasional perthitic
texture. All feldspars are strongly altered.
Lithic grains constitute on average about 40 %
of the total framework grains (Suppl. Table S1).
They are represented by metamorphic grains
(L
met
), volcanic grains (L
v
), grains of siliciclastic
sedimentary rocks (L
p
), and grains of carbonate
rocks (L
carb
). Grains of carbonate rocks include
mostly limestones, marly limestones, marls (L
lim
),
and dolomites (D).
The most common type of metamorphic grains
(Fig. 5B–E) are mica–quartz aggregates derived
from low- to medium-grade metamorphic rocks
Fig. 2. Lithostratigraphic column of the Oravic tectonic units of the PKB (after
Plašienka 2012a).
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Fig. 3. Classification of the sandstones studied based on their grain composition: A –– Pettijohn et al. (1972); B — Garzanti (2016). Black
dots — medium-grained sandstones; white circles — coarse-grained sandstones. Q — quartz, F — feldspar, L — lithic fragments including
lithoclasts of carbonates.
Fig. 4. Ternary provenance discrimination diagrams for the sandstones studied (fields after Dickinson & Suczek 1979; Dickinson 1985). Black
dots — medium-grained sandstones; white circles — coarse-grained sandstones. Q — quartz, Q
m
— monocrystalline quartz, Q
p
— polycrys-
talline quartz, F — feldspar, K — K-feldspar, L — lithoclasts including lithoclasts of carbonates, L
s
— sedimentary clasts, L
t
— total lithics
including carbonate lithoclasts, L
v
— volcanic clasts.
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(following discrimination criteria by Garzanti & Vezzoli
2003). Grains of low-grade metamorphic siliciclastic sedi-
mentary rocks (Fig. 5B–C) and grains of metabasic rocks also
occur. The amounts of metamorphic grains vary in the range of
0.0–26 %, (on average ~ 9 %) (Suppl. Table S1).
Grains of volcanic rocks occur in the subordinate amount of
1 % (Suppl. Table S1) and are represented mostly by basic
volcanic rocks (Fig. 5F).
Grains of siliciclastic sedimentary rocks constitute about
1 % of the whole-rock composition. Grains of carbonates of
the klippen succession provenance (Fig. 5B) are the most fre-
quent lithoclasts in the JPF, and their content varies in the range
from 0 to 64 % (on average of 21 %) (Suppl. Table S1).
Heavy mineral analysis
Almost all examined samples are characterized by a depleted
ultrastable association of heavy minerals (ZTR = zircon + tour-
maline + rutile). The heavy mineral associations are composed
either of prevailing ultrastable ZTR minerals over garnets and
apatites (zircon/tourmaline + garnet + apatite) or prevailing gar-
nets over ultrastable ZTR (garnet + zircon/tourmaline + apatite).
The Milpoš Breccia Mb. is characterized by the ultrastable
ZTR heavy mineral association (Table 2). Almost all the stu-
died samples contain detrital Cr-spinel (up to 13 %). Accessories
include epidote, sphene and minerals of the kyanite–silli-
manite–andalusite group.
Zircon (Fig. 6A–E) occurs mainly as colourless, yellow or
pink grains, with abundant inclusions and zonation. Zircon is
represented by subhedral or euhedral grains or their broken
fragments. Subrounded to rounded grains are present in subor-
dinate amount. Short stubby grains with crystal elongation
(length-to-width ratio) ~2–2.5:1 are most frequent (Fig. 6A).
Long prismatic and needle-shape grains (length-to-width
ratio >4:1) occur as well.
Tourmaline grains (Figs. 6F–I, 7A–H) are present mostly as
euhedral and angular broken fragments prevailing over sub-
rounded to rounded grains. The euhedral varieties very often
contain inclusions of zircon. Angular and subrounded grains
show initial to advanced stages of corrosion, mainly around rims
of grains (Andò et al. 2012) (Fig. 6H). Well rounded grains occur
only sporadically. Bright to dark brown to olive green coloured
grains predominate. Dark green or blue varieties are less fre-
quent. Salmon pink, colourless or zonal varieties are rare.
Rutiles occur as small mostly subrounded grains and sub-
hedral or prismatic fragments (Fig. 6K–L). Yellow, red and
Locality
Sample
GPS
Litostratigraphy
Macroscopic features
N
E
Litmanová
LIT-1
49˚ 22.547’
20˚ 37.228’
Milpoš Breccia Mb. Šariš Unit
medium/coarse-grained sandstone matrix of
coarse-grained carbonate breccia
Hajtovka
H-1B
49˚ 17.833’
20˚ 47.002’
Milpoš Breccia Mb. Šariš Unit
medium/coarse-grained sandstone matrix of
coarse-grained carbonate breccia
Kyjov
KYJ-1
49˚ 13.115’
20˚ 57.861’
Milpoš Breccia Mb. Šariš Unit
medium/coarse-grained sandstone matrix of
coarse-grained carbonate breccia
Milpoš
MIL-2
49˚ 11.824’
21˚ 00.204’
Milpoš Breccia Mb. Šariš Unit
medium/coarse-grained sandstone matrix of
coarse-grained carbonate breccia
Púchov
PU-5
49˚ 06.125’
18˚ 16.798’
Jarmuta–Proč Fm. Šariš Unit
(Javorina Beds Biele Karpaty Unit sensu Potfaj, 1993)
medium-grained sandstone
Sztolnia
SZTOL-1
49˚ 24.021’
20˚ 31.489’
Jarmuta–Proč Fm Šariš (Grajcarek) Unit
coarse-grained sanstone/fine-grained
conglomerate
Hajtovka
H-15
49˚ 18.101’
20˚ 45.192’
Jarmuta–Proč Fm Šariš Unit
coarse-grained sanstone/fine-grained
conglomerate
Olejníkov
DRA-B3
49˚ 11.543’
21˚ 03.033’
Jarmuta–Proč Fm Šariš Unit
medium-grained sandstone
Kračúnovce
KRC-5
49˚ 04.768’
21˚ 28.276’
Jarmuta–Proč Fm Šariš Unit
medium/coarse-grained sandstone matrix of
coarse-grained carbonate breccia
Beňatina
BEN-5
48˚ 48.922’
22˚ 20.799’
Jarmuta–Proč Fm Šariš Unit
medium/coarse-grained sandstone matrix of
coarse-grained carbonate breccia
Table 1: List of sampled sites for heavy mineral analysis, with their geographic coordinates, lithostratigraphy and macroscopic description.
Sample
Heavy mineral content [%]
Zrn
Tu
Rt
Grt
Ap
Sp
Ep
Ttn
Ky–Sil–And
ZTR
LIT-1
16
14
2
34
24
3
7
0
0.0
32
H-1B
24
13
10
24
16
12
0
0
0.9
48
KYJ-1
43
14
16
14
8
3
1
0
0.0
73
MIL-2
17
19
8
29
21
3
0
2
0.0
45
PU-5
28
8
9
47
7
1
0
0
0.0
45
SZTOL-1
27
6
7
50
6
6
0
0
0.0
39
H-15
14
16
6
25
33
4
0
3
0.0
36
DRAB-3
40
11
18
20
3
8
0
0
0.0
69
KRČ-5
28
6
11
46
4
4
1
0
0.0
45
BEN-5
4
8
5
70
8
1
2
0
0.4
18
Table 2: Frequencies of individual heavy minerals in the sediments studied. Abbreviations of minerals (Whitney & Evans 2010): Zrn — zircon,
Tur — tourmaline, Rt — rutile, Grt — garnet, Ap — apatite, Spl — spinel, Ep — epidote, Ttn — titanite (sphene), Ky — kyanite, Sil — silli-
manite, And — andalusite.
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orange varieties are very frequent. Some rutiles show initial
features of corrosion (Andò et al. 2012).
Garnet is represented by angular to subrounded fragments
(Figs. 6M–O, 7I–L). Well-rounded grains are very rare.
Colourless or salmon pink varieties dominate. Corrosion
features point to initial to advanced stages of weathering or
intrastratal dissolution (Andò et al. 2012).
Apatite is preserved either as colourless stubby euhedral
crystals (Fig. 6P) or as subrounded to rounded grains. Apatites
often show initial features of corrosion (Andò et al. 2012).
Spinel occurs mostly as reddish brown angular, subangular
to subrounded irregular fragments with characteristic con-
choidal breakage patterns (Fig. 6R–S).
Mineral chemistry
Chemistry of detrital tourmalines
The microprobe analysis reveals homogeneous chemistry of
the detrital tourmalines. The dominant cation occupying
the X-site is Na with a content in the range of 0.44–0.94 apfu.
Contents of Ca usually display values lower than 0.2 apfu.
The content of K is very low, not exceeding 0.1 apfu (Suppl.
Table S2). The X-site vacancy values do not exceed 0.46 apfu,
pointing towards the Alkali tourmaline subgroup (Fig. 8A).
Dominant divalent cations in the Y-site positions are Fe and
Mg. Their concentrations as well as the Mg / (Mg + Fe
tot
) ratio
values vary in the range of 0.3–0.8. Therefore, the analysed
tourmalines can be attributed to the schorl-dravite series
(Fig. 8B).
Characteristic for the studied tourmalines are common
growth zonations (Fig. 7B–G). Inclusions, mainly of zircon,
rutile, and xenotime are also a quite common feature in
the analysed tourmalines (Fig. 7H).
We used the provenance Al–Fe
tot50
Al
50
–Mg
50
Al
50
and
Ca–Fe
tot
–Mg diagrams (Henry & Guidotti 1985), where, based
on relative contents of the four most important substituent ele-
ments namely Al, Fe, Mg, and Ca, it is possible to distinguish
several various parent rock types (Fig. 9). The analysed det-
rital tourmalines were derived mainly from metapelites or
metapsamites and only few can be linked to granitoid rocks
and associated pegmatites.
Based on the Fe# value it is possible to discriminate tourma-
lines derived from granitoid rocks (0.8–1.0), hydrothermal
vein systems, or metasedimentary rocks (0.4–0.6) (Henry &
Guidotti 1985; Henry & Dutrow 1996). The Fe# of the ana-
lysed detrital tourmalines varies in the range of 0.31–0.83.
Chemistry of detrital garnets
The analysed detrital garnets show considerable variations
in the chemical composition (Fig. 10, Suppl. Table S3).
According to the chemical variations, the analysed garnets can
be divided into six different groups:
• The first group is represented by garnets with a high content
of the pyrope molecule (25–37 mol. %), a high content of
grossular (18–24 mol. %) and almandine (43–53 mol. %)
and a low content of spessartine (˂ 2 mol. %).
• Garnets belonging to the second group are characterized
by a high content of pyrope (39 mol. %) and almandine
(56 mol. %) and low contents of the grossular (3 mol. %)
and spessartine (~1 mol. %) molecules.
• The third group of garnets is characterized by a high content
of almandine (66–74 mol. %), a moderate content of pyrope
Fig. 5. Types of lithoclasts of the JPF: A — medium-grained quartzo–lithic arenite; B — coarse-grained sandstone to fine-grained conglomerate
composed of lithoclasts of limestones (L
lim
), dolomites (D), psephitic and psammitic clastic rocks (L
p
) and metamorphic rocks (L
met
);
C–E — lithoclasts of metamorphic rocks; F — clast of a basic volcanic rock. All photographs taken under crossed polars.
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MADZIN, PLAŠIENKA and MÉRES
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(16–27 mol. %), and low grossular (˂4 mol. %) and spessar-
tine (˂7 mol. %) contents.
• The fourth group is represented by a low content of spes-
sartine molecule (8 mol. %) and lower content of almandine
(54 mol. %) and pyrope (13 mol. %) and a higher content of
the grossular molecule (25 mol. %) than the previous group.
• Most of the analysed garnets have a high content of
the almandine molecule (46–82 mol. %), a variable content
of spessartine (1–50 mol. %), low pyrope (˂14 mol. %) and
low grossular (˂11 mol. %) contents.
• The last group is represented by garnets with the slightly
lower content of almandine (35–74 mol. %) and spessartine
(˂37 mol. %) and higher content of grossular (14–26 mol. %)
than the previous group, while the content of pyrope is low
(˂6 mol. %).
All of the analysed garnets contain very low uvarovite
and andradite amounts of ˂0.3 mol. % and ˂3 mol. %,
respectively.
Inclusions in the analysed garnets are most often repre-
sented by quartz, epidote and biotite (Fig. 7I–L).
Fig. 6. Characteristic heavy minerals selected from the sediments studied: A–E — colourless euhedral to rounded zircons with inclusions;
F –– euhedral tourmaline; G — broken prisms of subhedral tourmaline; H — initial to advanced features of corrosion around rims of angular
tourmaline; I, J — variously coloured rounded tourmalines; K, L — orange and lemon yellow subrounded rutiles; M–O — colourless angular
to subrounded garnets with facets on the surface of grains; P — subrounded apatite; R, S — grains of unaltered fresh Cr-spinels.
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Fig. 7. Back-scattered electron (BSE) images of the separated detrital heavy minerals for the mineral chemistry study. Abbreviations of mine-
rals (Whitney & Evans 2010): Qz — quartz, Bt — biotite, Ms — muscovite, Chl — chlorite, Xtm — xenotime, Ky — kyanite, Ep — epidote.
Explanations: Grt#24, Tur#36 — numbers of the analyses in the Supplement.
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Chemistry of detrital Cr-spinels
Based on the variability of the TiO
2
content and the Fe
2+
/Fe
3+
ratio it is possible to distinguish the upper mantle or volcanic
origin of spinels (Lenaz et al. 2000; Kamenetsky et al. 2001).
Upper mantle spinels are generally characterized by a low
TiO
2
content (˂0.2 wt. %). Their Fe
2+
/Fe
3+
ratio is higher than
two (˃2), within the overall range of Al
2
O
3
. Volcanic spinels
exhibit low TiO
2
value only in very rare cases (e.g., some low
TiO
2
MORB basalts, tholeiites or boninites, Kamenetsky et al.
2001). The amount of TiO
2
of the analysed spinels varies in
the range of 0.02–0.31 wt. % (Suppl. Table S4). A few spinels
show higher TiO
2
contents (3.26 wt. %), but it is rather a ref-
lection of initial alteration phases (the spinels also exhibit low
contents of Al
2
O
3
and MgO and a higher content of Fe
2
O
3
)
than primary crystallization conditions (cf. Mikuš & Spišiak
2007).
The content of Al
2
O
3
in the JPF vary in the range of
6.8–51.6 wt. % (Suppl. Table S4). Contents of TiO
2
and Al
2
O
3
in spinels are controlled by the parent magma, so they are good
indicators of their parent rocks (Kamenetsky et al. 2001). Based
on the content of oxides, sources of upper mantle spinels can
be divided into two groups, namely supra-subduction perido-
tites (SSZ peridotites; low Al
2
O
3
content) and MORB perido-
tites (high Al
2
O
3
content) (Fig. 11A). Contents of Cr
2
O
3
vary
in the JPF in the range of 17.6–55.7 wt. %. (Suppl. Table S4).
Most of the spinels show values of the Cr# = (Cr/Cr +Al) and
the Mg# = (Mg/Mg +Fe
2+
) in the range of 50–80 mol. % and
39–70 mol. %, respectively. According to the Cr# and Mg#,
the analysed spinels belong to mantle peridotites (Lenaz et al.
2000). In the Cr# vs. Mg# discrimination diagram (Dick &
Bullen 1984; Pober & Faupl 1988) (Fig. 12), the analysed
spinels mainly plot in the central area of the diagram, where
the fields largely overlap. A large majority of the analysed
spinels show the Cr# in the range of 50–65, which is adequate
to the type II peridotites (harzburgites). Some of the spinels of
the JPF show lower values of the Cr# and higher values of
the Mg#, including them in the type I peridotites (lherzolites)
(Dick & Bullen 1984) (Fig. 12).
Besides the low TiO
2
, the analysed spinels are also charac-
terized by the low Fe
3+
and by variable contents of Cr and Al.
In the ternary Cr–Al–Fe
3+
diagram (Fig. 11B), almost all
spinels plot along a Cr–Al trend. The Cr–Al trend is defined as
a relation of the Cr/(Cr+Al) vs. Fe
2+
/(Mg+Fe
2+
) typical for
mantle and lower crustal rocks (e.g., upper mantle xenoliths,
ophiolites, mid-ocean peridotites) (Barnes & Roeder 2001).
Discussion
Modal composition and heavy mineral assemblage
The modal composition of the studied sandstones suggests
their supracrustal provenance. The high amount of carbonate
clastic material, the low feldspar and the low volcanic clast
content together with the character of metamorphic clasts
point to a source area composed mainly of carbonate sedimen-
tary rocks and low- to medium-grade metamorphic rocks.
According to the discrimination diagrams of Dickinson &
Suczek (1979) and Dickinson (1985) such compositions are
related to source areas of a recycled collisional orogen (Fig. 4).
In our case the Q
m
FL
t
diagram seems to be more appropriate
than the QFL diagram of Dickinson (1985) since a conside-
ration of carbonate clasts to the L pole lead to an undissected
arc provenance (cf. von Eynatten & Gaupp 1999). Because
the sandstone composition is size dependent (Ingersoll et al.
1984), the individual size fractions were plotted separately
(Figs. 3, 4). The medium-grained sandstones plot closer to
Fig. 8. Classification of basic tourmaline groups; based on dominant occupancy at the X-site (Henry et al. 2011).
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Fig. 10. Ternary pyrope–almandine–grossular and pyrope–almandine–spessartine provenance diagrams (Méres 2008; Aubrecht et al. 2009).
Explanations: A — Grt derived from UHP/HP metamorphic conditions; position around number 1 — Grt derived from UHP eclogites, garnet
peridotites and kimberlites; B — Grt derived from granulite and eclogite facies conditions; position around number 2 — Grt derived from HP
eclogites and HP mafic granulites; position around number 3 — Grt derived from HP felsic and intermediate granulites; C — Grt derived from
amphibolite facies conditions; C1 — Grt derived from transitional high amphibolite to granulite facies conditions; position around
number 4 — Grt derived from gneisses metamorphosed under transitional high amphibolite to granulite facies conditions; position around
number 5 — Grt derived from amphibolites metamorphosed under transitional high amphibolite to granulite facies conditions; C2 — Grt
derived from amphibolite facies conditions; position around number 6 — Grt from gneisses metamorphosed under amhibolite facies condi-
tions; position around number 7 — Grt from amphibolites metamorphosed under amphibolite facies conditions. Grey fields — immiscibility
gap of end members composition.
Fig. 9. Compositional provenance diagrams for tourmalines: A — ternary Al–Fe
(tot)
–Mg diagram; B — ternary Ca–Fe
(tot)
–Mg diagram (Henry
& Guidotti 1985).
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the Q pole than coarse-grained sandstones, reflecting their
more distal deposition from the source, low resistance of car-
bonate clasts and/or disintegration of polycrystalline quartz
aggregates into monocrystalline quartz grains due to mecha-
nical abrasion during transport.
Collisional orogens provide huge amounts of detrital mate-
rial derived from a great variety of rock types and multiple
recycling of variegated material from older sedimentary forma-
tions incorporated into a prograding orogenic wedge. The ratio
of ultrastable zircon, tourmaline and rutile to all transparent
heavy minerals in siltstones/sandstones, i.e. the ZTR index,
is used to get information about a possible recycling of clastic
material and maturity of sediments (Hubert 1962). The ZTR
index in the studied sandstones ranges from 18 to 73 (Table 2).
Accordingly, considerable amounts of the detrital material
could have been recycled from older sedimentary formations.
On the other hand, the prevalence of euhedral to subhedral
habit of ultrastable heavy minerals combined with a high pro-
portion of lithic carbonate clasts suggest rather local sources
and a relatively shorter transport. Consequently, the modal
composition of the studied sediments, together with the heavy
mineral assemblage, points to a mixed provenance of the detri-
tal material, but still from local sources. One source can be
determined by the presence of the first-cycle derived carbo-
nate material, poor-rounded ZTR, Grt and Cr-spinels. Another
source can be deduced by the presence of the well-rounded
resistant clastic material coupled with the subrounded to
rounded ultrastable ZTR and Cr-spinels delivered from older
sedimentary formations.
As the less stable mineral phases such as epidote and sphene
were identified, though in a minor amount, a more diverse
original heavy mineral assemblage might be assumed. Less
stable minerals were most probably eliminated due to
mecha nical abrasion and weathering during transport and/or
intra stratal dissolution during burial diagenesis (Morton &
Hallswoth 1999, 2007; Turner & Morton 2007).
Origin of detrital tourmalines
The chemical composition of analysed detrital tourmalines
reveals their derivation mostly from low- to medium-grade
metamorphic rocks and to a lesser extent from granitoid rocks
(Fig. 9). A similar chemical composition of detrital tourma-
lines has been reported from the Lower Jurassic deposits of
the PKB in the Orava region and from the Lower Jurassic
deposits of the Tatric Unit of the CWC in the Malé Karpaty Mts.
(Aubrecht 1994; Aubrecht & Krištín 1995). A very large
amount of the detrital tourmalines in deposits of the Klape and
Manín units were derived, besides metasediments, also from
granitoid rocks (Aubrecht 2001). It has been hypothesized that
a source of the tourmalines might have been an area composed
of metamorphic and granitoid rocks, situated to the north of
the Tatric realm, supplying detrital material to both the Lower
Jurassic Tatric deposits to the south and to the Lower Jurassic
Oravic deposits to the north (Aubrecht 2001). The sources of
detrital tourmalines were also assumed to be in metamorphic
rocks of the CWC tectonic units, but because of either the very
low concentration of tourmalines in that rocks or a conside-
rably large distance to the final deposition place, these sources
seem to be very unlikely (cf. Aubrecht 1994; Aubrecht &
Krištín 1995 and references therein). If we assume crystalline
rocks of the CWC as the source of detrital tourmalines, they
should have experienced several sedimentary cycles, resulting
in a more advanced rounding of detrital grains, which is not
the case. For example, compositionally similar but predomi-
nantly well-rounded tourmalines have been reported from
Fig. 11. A — The Al
2
O
3
vs. TiO
2
discrimination diagram of compositional relationships in spinels (from Kamenetsky et al. 2001).
B — The Cr–Al–Fe
3+
ternary plot with the main relationship trends in spinel compositions (spinel gap field after Barnes & Roeder 2001).
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Upper Cretaceous and Oligocene flysch deposits of the EWC
(Salata & Uchman 2013; Salata 2014). Crystalline rocks of
the Bohemian Massif and/or basement rocks of Bruno-
vistulicum have been interpreted as their primary sources.
These rocks had supplied the Upper Palaeozoic and partly
Mesozoic clastic rocks deposited on the Silesia and Małopolska
blocks, later becoming the ultimate source for flysch deposits
of the Skole Basin (Salata 2014). Consequently, the majority
of detrital tourmalines in clastic deposits of the PKB units
were most probably derived from primary source rocks
situated in more proximal areas represented by supracrustal,
mainly low- to medium-grade metamorphic rocks either of
the Oravic ribbon continent or more external parts of the CWC
(cf. Aubrecht 2001).
Origin of detrital garnets
Detrital garnets from the studied rocks exhibit a conside-
rable variability of chemical composition suggesting their ori-
gin in various parent rocks types. The analysed garnets were
derived mainly from amphibolite metamorphic facies rocks,
transitional amphibolite to granulite facies rocks or from retro-
grade eclogites, and from HP/HT granulites and eclogites.
At five studied localities, almandine type garnets prevail.
They were most probably derived from gneisses and amphi-
bolites originated under amphibolite facies metamorphic
conditions. Garnets of this composition were also reported
from HP/LT metamorphic rocks and metabasic rocks
(blueschist facies rocks), skarns, contact metamorphic rocks,
migmatites and various types of granitoid rocks (see Méres
2008; Aubrecht et al. 2009). However, we have not observed
index minerals of HP/LT metamorphism. Detrital garnets,
dominantly of almandine composition, have also been reported
from the Maastrichtian–Palaeocene Jarmuta Fm. of
the Graj
carek Unit and from the Coniacian–Santonian
Sromowce Fm. of the Branisko Unit of the PKB in Poland
(Salata 2004). Detrital garnets of a similar composition also
occur in Jurassic deposits of the CWC nappe units. Their
source rocks have been regarded as low- to medium-grade
metamorphic rocks of the CWC crystalline basement
(Aubrecht & Méres 2000).
At the two localities from the eastern part of the PKB,
detrital garnets with a higher content of the pyrope molecule
(<39 %) were revealed in the heavy mineral assemblage
(Suppl. Table S3). The chemical composition of these garnets
suggests their derivation from granulites (Fig. 10 sector C1
Fig. 12. The Cr# vs. Mg# bivariate plots of calculated cation ratios Cr/(Cr+Al) vs. Mg/(Mg+Fe
2+
) (the discrimination fields after Dick & Bullen
1984; Pober & Faupl 1988).
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MADZIN, PLAŠIENKA and MÉRES
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number 4) and amphibolites and/or retrograde eclogites meta-
morphosed under transitional amphibolite to granulite facies
conditions (Fig. 10 sector C1 number 5). Garnets with
a high content of pyrope and grossular and with a low content
of spessartine were derived from eclogites or mafic granulites
(Fig. 10 sector B number 2). Garnets with a high content of
pyrope and almandine but a low content of grossular and spes-
sartine originated in felsic to intermediate granulites (Fig. 10
sector B around number 3). Garnets of similar composition
(pyrope–almandine and pyrope–almandine–grossular) prevail
in heavy mineral assemblages of Jurassic deposits (Aubrecht
& Méres 2000) and also in the Albian deposits of the Czorsztyn
succession of the PKB (Aubrecht et al. 2009). They have also
been reported in the Cretaceous and Palaeogene flysch depo-
sits of the EWC (Otava et al. 1998; Salata 2004; Oszczypko &
Salata 2005; Grzebyk & Leszczyński 2006). There is a lack of
pyrope–almandine garnets in crystalline basement rocks of
the CWC and Internal WC (IWC) (Aubrecht & Méres 2000
and references therein). Accordingly, the HP/HT granulite and
eclogite facies rocks of the ancient Oravic ribbon continent
(or Czorsztyn Ridge) are assumed to have been a source of
pyrope–almandine garnets within the Jurassic and Cretaceous
sediments of the PKB. This continental fragment was derived,
most probably, from the Moldanubian Zone of the Bohemian
Massif by rifting during the Middle Jurassic (Aubrecht &
Méres 2000; Aubrecht et al. 2009).
Another explanation, which should be taken into conside-
ration, is that high-pyrope garnets could have been derived
from sub-ophiolitic high-grade metamorphic soles developed
in SSZ settings of the Meliata–Vardar oceanic realm (e.g.,
Lužar-Oberiter et al. 2008; Mikes et al. 2008; Stern &
Wagreich 2013). The dominance of mostly harzburgitic (SSZ
peridotites) detrital Cr-spinels may support this model.
As indicated by generally poor roundness of detrital garnets,
a more proximal primary source should be assumed. The high-
pyrope garnets could have been derived from HT/HP felsic or
mafic granulite and eclogite facies rocks of a lower crust
exhumed during formation of the Vahic oceanic basin, which
were later incorporated into the prograding CWC orogenic
wedge in the uppermost Cretaceous to Palaeogene times.
Palaeotransport directions reported from the Jarmuta Fm. in
the Polish part of the PKB show that detrital material was
delivered mainly from SE (Salata 2004; Oszczypko & Salata
2005). Unfortunately, palaeotransport directions collected
during our study could not be used for the identification of
source areas due to poor outcrop conditions and problematic
tectonic restoration. Nevertheless, our measured data roughly
agree with the palaeotransport of detrital material from SE
towards NW. However, the reported palaeocurrent data have
not been corrected for the Miocene united ~50–60˚ counter-
clockwise (CCW) rotation of the Alcapa block revealed by
the palaeomagnetic studies of the Flysch Belt, PKB and
Central Carpathian Palaeogene Basin (Márton et al. 2009a, b,
2013). If the Miocene CCW rotation is taken into account
a general palaeotransport of detrital material from S/SWS
towards N/NEN is indicated (Fig. 13).
In the eastern part of the WC, the continuation of the Vahic
oceanic system is thought to be the Iňačovce–Kričevo remnant
oceanic basin (Soták et al. 1993, 1994, 2005; Plašienka &
Soták 2015; Kováč et al. 2016). While subduction of the Vahic
oceanic or thinned continental crust ceased at the Cretaceous/
Palaeogene boundary on the western part of the WC,
the Iňačovce–Kričevo remnant basin was still active till
the end of the Eocene on the east (Soták et al. 1994, 2005;
Kováč et al. 2016). Therefore, this southerly situated realm
(before Miocene rotation) could have provided a source of
high-pyrope garnets (Fig. 13). In the western part of the PKB,
these sources were already eroded and did not exist during
deposition of the JPF, since it contains only almandine garnets
derived from accreted low- to medium-grade metamorphic
rocks of the Oravic ribbon continent.
Origin of detrital Cr-spinels
In the PKB s.l., the first occurrence of detrital Cr-spinels has
been revealed in the Barremian–Aptian pebble material of
the Albian exotic conglomerates of the Klape Unit and in equi-
valent Coniacian–Santonian conglomerates of the Pieniny Unit
(Mišík et al. 1980). A relatively high content of Cr-spinels has
been reported from condensed, red marly sediments with clas-
tic admixtures of the Albian Chmielowa Fm. of the Czorsztyn
succession (Aubrecht et al. 2009). Significant amounts of
Cr-spinels were found in the Upper Cretaceous to Palaeocene
flysch deposits of the Grajcarek and Branisko units of the PKB
Fig. 13. Schematic palaeogeographic situation of the Pieniny Klippen
Belt during Palaeocene–Lower Eocene (based on Soták et al. 1994,
2005; Plašienka & Soták 2015; Kováč et al. 2016). CWC — Central
Western Carpathians; PKB — PieninyKlippen Belt; I–K — Iňačovce–
Kričevo remnant oceanic basin; ZTR-f — first-cycle poor-rounded
ultrastable minerals; ZTR-r — recycled well-rounded ultrastable
mine rals; Grt-alm — almandine garnets from low- to medium-grade
metamorphic rocks; Grt-prp — pyrope–almandine garnets from high-
grade metamorphic rocks; Cr-harz — Cr-spinels of harzburgitic
origin; Cr-lherz — Cr-spinels of lherzolitic origin
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in southern Poland (Winkler & Ślączka 1992, 1994; Salata
2002, 2004; Oszczypko & Salata 2005). The pebble material
(Mišík et al. 1991) and sandstones (Bónová et al. 2018) of
the Palaeogene Proč Conglomerates from eastern Slovakia
contain Cr-spinels as well.
The source of the ophiolitic detritus in clastic deposits of
the PKB has been generally considered to be the same as for
the material of the exotic conglomerates of the Klape Unit (for
comprehensive review see e.g., Mišík & Marschalko 1988;
Dal Piaz et al. 1995; Aubrecht et al. 2009; Plašienka 2012a;
Plašienka & Soták 2015). An exotic or cryptic (totally
destroyed or buried) ridge, known as the Pieniny Ridge
(Andrusov 1938, 1945; Mišík & Sýkora 1981; Mišík &
Marschalko 1988), or the Andrusov Ridge (Birkenmajer 1988)
has been suspected to be the source of the exotic material.
The Andrusov Ridge was supposed to occupy the position
between the Kysuca–Pieniny (Vahic) sedimentary realm and
the external margin of the CWC units forming the accretionary
wedge created by the subduction of the Vahic Ocean (sensu
Maheľ 1981, 1989; Birkenmajer 1988). Accordingly, the Cr-
spinels in clastic sediments of the PKB could represent ophio-
litic detritus of the completely consumed Vahic oceanic crust.
The Pieniny or Andrusov Ridge was interpreted as a compres-
sional structure (Mišík 1979; Birkenmajer 1988; Maheľ 1989),
therefore, it should have been situated on the active continen-
tal margin, although that is not in accordance with the Upper
Jurassic to Lower Cretaceous structural, magmatic and sedi-
mentary rock record. The Lower Jurassic to Lower Cretaceous
period was characterized by an extensional, and not a com-
pressional tectonic regime in the north Tatric realm (Plašienka
1995a, b, 1996). This assumption led to the alternative expla-
nation that the Klape Flysch represents an analogue to
the Albian– Cenomanian Poruba Flysch of the Tatric and Fatric
units of the CWC. Consequently, the Klape Unit might have
been derived from the Fatric Zliechov Basin. Therefore,
the varie gated detrital material and the ophiolitic detritus
could have come from source areas situated near the Veporic
Unit being uplifted and eroded due to the closure of the Meliata
Ocean in the Late Jurassic (Plašienka 1995a, b, 1996). Sub-
sequently, the nappe transport of the Fatric nappe system over
the Tatricum took place in the Turonian and the Klape Unit
gravitationally slid down to a false accretionary wedge posi-
tion externally to the north Tatric margin (Plašienka 1997,
1999, 2012a; Prokešová et al. 2012).
Another interpretation assumes that the Oravic ribbon con-
tinent was placed in the lateral continuation of the CWC and
IWC units, in a close vicinity to the Meliatic oceanic realm
during the Jurassic. Later, during the Early to middle Cre-
taceous, the Oravic ribbon continent was separated from its
original position, and due to a clockwise rotation of the entire
CWC (Aubrecht & Túnyi 2001) transported to the front of
the CWC, where together with the Meliatic ophiolite fragment
formed the Andrusov Ridge (Aubrecht et al. 2009; Bellová et
al. 2018). Such an assumed elevation, being created in a trans-
pressional tectonic shear zone instead of the contractional tec-
tonic regime (cf. Marschalko 1986), might have fed detrital
material and ophiolitic detritus to both the Klape and Oravic
basins as well as to the CWC Tatric and Fatric basins for
a long time (Aubrecht et al. 2009). Conversely, there is no
structural record of such a huge crustal block transport.
Moreover, the assumed palaeogeographical interpretation,
where the Oravic tectonic units are turned over 180°, means
that no basin existed between the Czorsztyn Ridge and CWC
units, while the Kysuca–Pieniny Basin was not connected to
the Vahic Basin but to the Magura Basin in a more external
position (Aubrecht et al. 2009, their figs. 12, 13).
Several authors proposed a recycling model of exotic
pebbles in the Senonian and Palaeogene conglomerates of
the WC, whereby most of their material was resedimented
from the mid-Cretaceous conglomerates of the Klape Flysch
(Birkenmajer 1988; Salaj 1991; Plašienka 1995a, 2012a;
Plašienka & Soták 2015; Plašienka et al. 2018). Thus, the same
pebble material can be found in the Coniacian–Santonian con-
glomerates of the Sromowce Formation of the Oravic Pieniny
Unit and then, in decreasing amounts, also in the Maastrichtian
Jarmuta Fm. and the Palaeogene Proč Fm. of the Šariš Unit.
Exotic pebbles have also been reported from the Senonian–
Eocene conglomerates of the Gosau Group in western
Slovakia. Hence, the problem of the exotic pebble material
does not only concern the primary source area, but is also
reflected by their presence in units within the PKB covering
a time span of ~ 60 Ma (Plašienka & Soták 2015).
The chemical composition of detrital Cr-spinels of the JPF
indicates erosion of a common source composed of a transi-
tional harzburgitic/lherzolitic type (the type II peridotite sensu
Dick & Bullen 1984; Pober & Faupl 1988). Chemical compo-
sitions of detrital Cr-spinels reported from individual tectonic
units of the WC show that there is a clear prevalence of
harzburgitic parent rocks. Harzburgites are characteristic for
the more southern Meliata–Vardar provenance as has been
interpreted from many clastic deposits throughout the Alpine–
Carpathian–Dinaridic orogenic system (e.g., Pober & Faupl
1988; Árgyelán 1996; von Eynatten & Gaupp 1999; Lužar-
Oberiter et al. 2008, 2012; Mikes et al. 2008; Missoni &
Gawlick 2011; Stern & Wagreich 2013; Gawlick et al. 2015).
On the other hand, the chemical compositions of Cr-spinels
derived from the Meliatic and Penninic ultramafic bodies of
the WC and eastern part of the Northern Calcareous Alps
(NCA) rather correspond to a lherzolitic composition of rocks
(Mikuš & Spišiak 2007). However, large alterations of Cr- spinels
due to serpentinization and/or low-grade metamorphism com-
plicating their discrimination were observed (Mikuš & Spišiak
2007; Koppa et al. 2014). Another problem may occur when
altered spinels are plotted in the discrimination diagrams of
Dick & Bullen (1984) and Kamenetsky et al. (2001). As shown
by Mikuš & Spišiak (2007), a number of their analyses plot
well within the field of SSZ peridotites or harzburgites (type
III peridotites). However, most of the fresh spinels correspond
to MORB peridotites or mostly to lherzolites (type I perido-
tites). If serpentinization has a significant effect on the chemis-
try of the in situ Cr-spinels, this will inevitably impact upon
the detrital spinel chemistry. Since provenance studies usually
30
MADZIN, PLAŠIENKA and MÉRES
GEOLOGICA CARPATHICA
, 2019, 70, 1, 15–34
rely on the 63–125 µm size fraction, the context of the grain
can be lost, especially in the case, where the entire grain is
altered or only an altered fragment is preserved (Mikuš &
Spišiak 2007). Problems concerning the validity of Cr-spinels
as reliable petrogenetic indicators have also been highlighted
in a study on the Rum layered intrusion in Scotland (Power et
al. 2000), where detrital spinels separated from sediments of
streams draining the ultramafic rocks show considerable
enrichment of Cr and Fe at the expense of Al. It is, therefore,
highly recommended to use discrimination diagrams with
more caution especially in the case of the Cr-spinels with
genuine higher Al content, which seem to be less resistant to
weathering, transport and diagenetic processes (see also Mikuš
& Spišiak 2007; Gawlick et al. 2015; Bónová et al. 2017,
2018; Bellová et al. 2018). Accordingly, it is very difficult to
differentiate between Penninic or Meliatic sources of ophio-
litic detritus based on the spinel chemistry alone (cf. Pober &
Faupl 1988; Stern & Wagreich 2013). Nevertheless, some
trend is visible in Cr-spinel compositions throughout the sedi-
mentary sequences of the PKB and CWC. Cr-spinels from
the Coniacian–Santonian Sromowce Formation of the Pieniny
Unit (our unpublished data) have the same harzburgitic origin
as those reported from the Albian–Cenomanian Klape Flysch
and analogous Poruba Fm. of the Tatric and Fatric tectonic
units (Jablonský et al. 2001; Mikuš et al. 2006; Lenaz et al.
2009; Bellová et al. 2018). This pattern fits very well with
the recycling model of the exotic pebble material and ophio-
litic detritus originated in more southern Meliatic realms as has
been proposed most recently by Plašienka (2012a), Plašienka
& Soták (2015) and Plašienka et al. (2018).
The occurrence of lherzolitic Cr-spinels in the Maastrichtian
to Lower/Middle Eocene JPF may suggest their delivery from
a different ophiolitic sequence, most probably of the Vahic
provenance. Similar changes in the proportional composition
of detrital Cr-spinels in time and space have been observed in
the Gosau Group sediments of the NCA and western part of
the WC (Stern & Wagreich 2013). In the Coniacian–Santonian
sediments, there is a dominance of harzbugitic over lherzo-
litic-spinels (75:14). The dominance of harzburgitic Cr-spinels
is reduced during Campanian and a considerable input of lher-
zolitic Cr-spinels is evident (53:41), while in the Maastrichtian–
Palaeocene sediments, harzburgitic Cr-spinels dominate
once again (63:30). Moreover, from the Campanian onwards,
the heavy mineral spectra of the Gosau Group sediments
record a dominant switchover from an ophiolite–dominated
source area to that composed chiefly of high-grade metamor-
phic rocks (Wagreich & Faupl 1994; Stern & Wagreich 2013).
The closure of the Vahic Ocean and the subsequent collision of
the Oravic ribbon continent with the frontal edge of the CWC
orogenic wedge has been roughly placed at the Cretaceous/
Palaeogene boundary (e.g., Plašienka 1997). Therefore, from
the Campanian onwards, obduction and erosion of the Vahic
ophiolites of the lherzolitic composition might have taken
place. The Penninic (Vahic) oceanic basin formation is asso-
ciated with the Jurassic to Early Cretaceous extension which
led to the exhumation of lower crustal high-grade metamorphic
rocks and subcontinental mantle rocks composed mostly of
lherzolites (e.g., Froitzheim & Manatschal 1996; Plašienka
2003; Manatschal & Münterer 2009). A lower crust composed
of felsic to mafic granulite and eclogite facies rocks might
then be a hypothetical source for the high-pyrope garnets
revealed in the eastern part of the PKB. The negative correla-
tion between detrital Cr-spinels and garnets (Stern & Wagreich
2013) may also support derivation of garnets rather from lower
crustal granulite/eclogite facies rocks than from sub-ophiolitic
high-grade metamorphic soles formed in SSZ settings of
the more southern Meliatic oceanic realm (e.g., Lužar-Oberiter
et al. 2008; Missoni & Gawlick 2011; Gawlick et al. 2015).
Although, the negative correlation may reflect the originally
very low (~2 %) concentration of Cr-spinels in their parent
rocks.
Conclusions
The origin of the synorogenic deposits of the PKB was rela-
ted to the collision of the ancient passive margins of the Vahic
Ocean, namely the Oravic ribbon continent in the more exter-
nal position and the CWC continental margin in the more
internal position. The main aim of this paper was to find out
how these deposits, through their composition, record infor-
mation about sources of detrital material. The main conclu-
sions of this paper are:
• The modal composition of the studied medium- to coarse-
grained sandstones of the Maastrichtian to Lower/Middle
Eocene Jarmuta–Proč Fm. classifies them mostly as quarzo-
lithic to lithic arenites.
• The character of the detrital material suggests its supra-
crustal provenance. The high amount of carbonate clastic
material, the low feldspar and the low volcanic clast content
together with the character of metamorphic clasts point to
a source area composed mainly of carbonate sedimentary
rocks and low- to medium-grade metamorphic rocks.
• The heavy mineral associations and the habitus of indivi-
dual heavy minerals point to a mixed provenance. One pri-
mary source is revealed by the presence of euhedral to
subhedral ultrastable ZTR, angular garnets and Cr-spinels.
It suggests erosion of mainly low- to medium-grade meta-
morphic rocks of the Oravic continental fragment. Another,
still local source, can be deduced by the presence of sub-
rounded to rounded ultrastable ZTR and Cr-spinels, recy-
cled from the older exotic conglomerates-bearing Sromowce
Fm. of the Pieniny Unit. These two sources can be observed
throughout the whole studied part of the PKB.
• The chemistry of detrital tourmalines points to their deriva-
tion mainly from low- to medium-grade metasedimentary
rocks with a minor contribution of granitoid rocks.
• The chemistry of detrital garnets shows the dominance of
almandine garnets derived from various types of low- to
medium- grade metamorphic rocks. The presence of high-
pyrope garnets in the eastern part of the PKB is striking.
The high-pyrope garnets may have originated in high-grade
31
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GEOLOGICA CARPATHICA
, 2019, 70, 1, 15–34
mafic and felsic granulites and eclogites representing most
probably a lower crust exhumed during the formation of
the Vahic oceanic basin in Jurassic to Lower Cretaceous
times. Later in the Upper Cretaceous to Palaeocene, frag-
ments of the high-grade metamorphic rocks were incorpo-
rated into the prograding CWC accretionary wedge and
provided local sources for the clastic material.
• The Cr-spinels of the Jarmuta–Proč Fm. suggest a mixed
harzburgitic and lherzolitic provenance. The harzburgitic
Cr-spinels might have been recycled from older exotic con-
glomerates of the Sromowce Fm. and Klape Flysch, thereby
representing ophiolitic detritus of the Upper Triassic–
Jurassic Meliata–Vardar Ocean. The lherzolitic Cr-spinels
might represent a new contribution of ophiolitic detritus
delivered from the exhumed subcontinental mantle forming
the Jurassic–Lower/Middle Cretaceous Vahic oceanic
floor.
Acknowledgements: We would like to thank reviewers Dorota
Salata and Wolfgang Knierzinger for their critical remarks and
useful suggestions, which helped to improve the quality of this
paper. The work of managing editor Milan Kohút and han-
dling editor Anna Vozárová is gratefully acknowledged. This
work was financially supported by the Slovak Research and
Development Agency (projects APVV-0212-12 and APVV-
17-0170) and by the VEGA Scientific Agency (projects VEGA
1/0388/10, VEGA 2/0028/17).
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i
PROVENANCE OF SYNOROGENIC DEPOSITS OF THE JARMUTA–PROČ FORMATION
GEOLOGICA CARPATHICA
, 2019, 70, 1, 15–34
Jarmuta–Proč Fm.
Sample
Q
m
Q
p
P
K
L
met
L
v
L
lim
D
L
p
Q
t
F
L
L
t
L
s
L
carb
L+L
carb
L
t
+L
carb
L
s
+L
carb
LIT-A10
64.8
11.3
4.2
2.6
0.0
0.3
11.6
0.0
5.2
76.1
6.8
5.5
16.8
5.2
11.6
17.1
28.4
16.8
LIT-A15
17.8
34.6
0.9
2.3
20.6
2.8
10.3
10.7
0.0
52.3
3.3
23.4
57.9
20.6
21.0
44.4
79.0
41.6
LIT-B5
56.4
18.4
5.1
13.2
1.3
0.0
0.0
1.7
3.8
74.8
18.4
5.1
23.5
5.1
1.7
6.8
25.2
6.8
LIT-B8
30.0
33.5
1.3
2.6
18.3
0.4
8.7
3.9
1.3
63.5
3.9
20.0
53.5
19.6
12.6
32.6
66.1
32.2
LIT-B9
13.1
9.5
0.0
1.5
14.6
0.0
31.7
28.6
1.0
22.6
1.5
15.6
25.1
15.6
60.3
75.9
85.4
75.9
LIT-B10
52.8
13.4
0.9
3.7
8.3
0.5
14.4
1.9
4.2
66.2
4.6
13.0
26.4
12.5
16.2
29.2
42.6
28.7
LIT-B11
24.8
22.2
1.7
3.4
18.4
0.4
17.1
9.0
3.0
47.0
5.1
21.8
44.0
21.4
26.1
47.9
70.1
47.4
LIT-B12
23.6
18.9
0.9
0.9
15.5
0.4
33.5
5.6
0.9
42.5
1.7
16.7
35.6
16.3
39.1
55.8
74.7
55.4
LIT-B13
44.3
18.3
0.9
10.4
11.7
0.4
9.1
2.6
2.2
62.6
11.3
14.3
32.6
13.9
11.7
26.1
44.3
25.7
LIT-B14
31.1
32.0
0.0
3.5
14.9
0.4
7.0
10.1
0.9
63.2
3.5
16.2
48.2
15.8
17.1
33.3
65.4
32.9
LIT-B15
16.9
37.3
0.4
3.6
18.2
0.9
8.0
14.2
0.4
54.2
4.0
19.6
56.9
18.7
22.2
41.8
79.1
40.9
LIT-B16
36.2
27.6
2.3
0.9
13.1
0.0
17.2
2.3
0.5
63.8
3.2
13.6
41.2
13.6
19.5
33.0
60.6
33.0
LIT-B17
44.3
20.1
2.0
7.4
8.6
0.4
15.2
1.2
0.8
64.3
9.4
9.8
29.9
9.4
16.4
26.2
46.3
25.8
LIT-B18
34.0
25.3
2.3
2.3
15.5
1.1
11.7
6.4
1.5
59.2
4.5
18.1
43.4
17.0
18.1
36.2
61.5
35.1
LIT-B19
34.5
12.5
0.5
6.0
9.5
2.0
29.0
3.5
2.5
47.0
6.5
14.0
26.5
12.0
32.5
46.5
59.0
44.5
L29
52.2
5.6
1.7
1.7
2.6
0.0
18.5
0.0
17.7
57.8
3.4
20.3
25.9
20.3
18.5
38.8
44.4
38.8
H-1A
42.9
14.2
0.9
2.7
11.0
0.5
25.6
1.4
0.9
57.1
3.7
12.3
26.5
11.9
26.9
39.3
53.4
38.8
H-1B
30.5
30.1
1.8
2.2
16.5
0.7
14.0
2.6
1.5
60.7
4.0
18.8
48.9
18.0
16.5
35.3
65.4
34.6
H-15
22.6
23.8
0.9
1.3
26.4
3.8
15.7
5.5
0.0
46.4
2.1
30.2
54.0
26.4
21.3
51.5
75.3
47.7
SJ-1A
18.7
16.4
1.8
0.4
18.7
1.3
24.9
16.9
0.9
35.1
2.2
20.9
37.3
19.6
41.8
62.7
79.1
61.3
SJ-1B
20.8
31.7
0.0
0.0
2.5
1.7
20.0
21.7
1.7
52.5
0.0
5.8
37.5
4.2
41.7
47.5
79.2
45.8
SJ32-1
14.1
19.0
0.0
2.3
17.5
0.8
31.2
14.8
0.4
33.1
2.3
18.6
37.6
17.9
46.0
64.6
83.7
63.9
SJ32-2
25.3
21.0
1.1
2.2
8.6
3.2
29.0
7.5
2.2
46.2
3.2
14.0
34.9
10.8
36.6
50.5
71.5
47.3
KYJ1A
61.8
18.7
2.8
0.8
4.1
0.4
7.3
2.4
1.6
80.5
3.7
6.1
24.8
5.7
9.8
15.9
34.6
15.4
KYJ1B
28.6
31.5
0.5
1.4
9.4
0.0
12.2
16.4
0.0
60.1
1.9
9.4
40.8
9.4
28.6
38.0
69.5
38.0
KYJ4-1
41.9
23.9
0.0
2.3
4.1
3.6
17.1
6.8
0.5
65.8
2.3
8.1
32.0
4.5
23.9
32.0
55.9
28.4
KYJ4-2
35.7
16.2
0.5
3.3
9.5
1.0
27.1
6.2
0.5
51.9
3.8
11.0
27.1
10.0
33.3
44.3
60.5
43.3
MILPOS-A
30.0
27.4
1.8
7.6
12.6
1.3
8.5
10.3
0.4
57.4
9.4
14.3
41.7
13.0
18.8
33.2
60.5
31.8
MILPOS-B
28.7
22.8
2.1
3.8
11.0
1.7
18.6
11.0
0.4
51.5
5.9
13.1
35.9
11.4
29.5
42.6
65.4
40.9
MILPOS-C
26.4
24.7
6.3
5.6
12.8
2.8
15.3
6.3
0.0
51.0
11.8
15.6
40.3
12.8
21.5
37.2
61.8
34.4
MIL-1A
49.8
10.0
3.5
8.3
5.7
0.9
20.5
0.0
1.3
59.8
11.8
7.9
17.9
7.0
20.5
28.4
38.4
27.5
MIL-1C
52.8
19.1
1.2
1.6
2.8
0.8
18.3
2.0
1.2
72.0
2.8
4.9
24.0
4.1
20.3
25.2
44.3
24.4
MIL-1D
44.6
22.7
1.2
3.3
5.8
0.8
10.7
8.7
2.1
67.4
4.5
8.7
31.4
7.9
19.4
28.1
50.8
27.3
MIL-1E
67.9
8.5
0.8
0.8
3.3
0.4
17.5
0.0
0.8
76.4
1.6
4.5
13.0
4.1
17.5
22.0
30.5
21.5
MIL-2A
56.3
9.7
0.0
1.9
6.8
0.0
20.9
0.0
4.4
66.0
1.9
11.2
20.9
11.2
20.9
32.0
41.7
32.0
MIL-2B
75.2
4.8
1.3
1.3
1.7
0.0
14.8
0.0
0.9
80.0
2.6
2.6
7.4
2.6
14.8
17.4
22.2
17.4
MIL-5A
47.3
16.5
1.2
3.3
6.2
0.8
22.2
2.1
0.4
63.8
4.5
7.4
23.9
6.6
24.3
31.7
48.1
30.9
MIL-5B
42.2
17.1
1.6
2.7
4.7
1.2
25.6
2.7
2.3
59.3
4.3
8.1
25.2
7.0
28.3
36.4
53.5
35.3
MIL-6
24.1
19.9
1.2
3.7
10.4
1.7
28.6
10.4
0.0
44.0
5.0
12.0
32.0
10.4
39.0
51.0
71.0
49.4
DRA-A1
45.0
20.2
0.4
0.0
10.3
0.0
22.7
0.4
0.8
65.3
0.4
11.2
31.4
11.2
23.1
34.3
54.5
34.3
DRA-A2
18.4
15.2
0.0
0.9
11.2
0.0
23.8
30.5
0.0
33.6
0.9
11.2
26.5
11.2
54.3
65.5
80.7
65.5
DRA-A4
53.4
9.2
1.2
0.4
4.4
0.0
29.3
1.2
0.8
62.7
1.6
5.2
14.5
5.2
30.5
35.7
45.0
35.7
DRA-A7
36.9
4.4
2.0
1.5
6.9
0.5
45.3
1.5
1.0
41.4
3.4
8.4
12.8
7.9
46.8
55.2
59.6
54.7
DRA-B1
60.4
15.2
1.4
0.0
3.2
0.4
14.5
0.7
4.2
75.6
1.4
7.8
23.0
7.4
15.2
23.0
38.2
22.6
DRA-B2
59.4
11.3
0.4
2.3
5.6
0.0
16.9
1.9
2.3
70.7
2.6
7.9
19.2
7.9
18.8
26.7
38.0
26.7
DRA-B3
45.7
15.6
1.1
0.7
13.0
0.4
18.1
2.5
2.9
61.2
1.8
16.3
31.9
15.9
20.7
37.0
52.5
36.6
DRA-B4
49.8
13.2
1.3
1.3
12.8
0.4
17.2
2.2
1.8
63.0
2.6
15.0
28.2
14.5
19.4
34.4
47.6
33.9
DRA-B5
53.9
16.0
0.8
1.6
7.4
0.0
16.0
2.7
1.6
69.9
2.3
9.0
25.0
9.0
18.8
27.7
43.8
27.7
DRA-B6
63.6
8.9
2.3
1.2
5.8
0.0
13.6
3.5
1.2
72.5
3.5
7.0
15.9
7.0
17.1
24.0
32.9
24.0
DRA-B7
50.4
15.8
0.9
0.4
12.4
0.0
16.2
2.6
1.3
66.2
1.3
13.7
29.5
13.7
18.8
32.5
48.3
32.5
DRA-B8
48.8
15.2
0.4
1.2
12.8
0.4
16.4
1.6
3.2
64.0
1.6
16.4
31.6
16.0
18.0
34.4
49.6
34.0
DRA-B9
36.0
19.3
0.8
0.8
14.8
0.4
17.8
9.5
0.8
55.3
1.5
15.9
35.2
15.5
27.3
43.2
62.5
42.8
DRA-B10
26.7
25.5
0.0
0.0
14.2
0.8
21.1
11.7
0.0
52.2
0.0
15.0
40.5
14.2
32.8
47.8
73.3
47.0
DRA-B11
24.7
26.4
0.4
0.8
14.6
0.4
18.0
14.6
0.0
51.0
1.3
15.1
41.4
14.6
32.6
47.7
74.1
47.3
DRA-B14
63.1
13.1
0.7
0.7
3.7
0.0
14.2
0.7
3.7
76.1
1.5
7.5
20.5
7.5
14.9
22.4
35.4
22.4
DRA-B16
59.5
14.9
0.4
1.1
7.8
0.4
13.8
0.0
2.2
74.3
1.5
10.4
25.3
10.0
13.8
24.2
39.0
23.8
DRA-B20
60.8
7.8
0.8
2.7
2.0
0.0
19.2
3.5
3.1
68.6
3.5
5.1
12.9
5.1
22.7
27.8
35.7
27.8
TR-3
30.3
17.0
0.0
1.7
12.0
0.0
27.8
10.8
0.4
47.3
1.7
12.4
29.5
12.4
38.6
51.0
68.0
51.0
TR-5A
34.9
15.5
0.0
0.4
7.8
0.0
26.0
14.3
1.2
50.4
0.4
8.9
24.4
8.9
40.3
49.2
64.7
49.2
TR-5B
49.6
11.5
0.8
1.2
6.3
0.4
25.4
4.4
0.4
61.1
2.0
7.1
18.7
6.7
29.8
36.9
48.4
36.5
DEM-4
31.5
21.0
0.7
1.1
9.7
1.5
22.8
10.9
0.7
52.4
1.9
12.0
33.0
10.5
33.7
45.7
66.7
44.2
DEM-5
36.2
23.6
0.0
0.0
7.4
4.4
11.8
16.6
0.0
59.8
0.0
11.8
35.4
7.4
28.4
40.2
63.8
35.8
TUL-3
19.3
4.7
0.5
0.0
1.9
0.5
67.9
4.7
0.5
24.1
0.5
2.8
7.5
2.4
72.6
75.5
80.2
75.0
TUL-4
27.9
7.9
0.5
0.5
6.3
1.6
44.2
11.1
0.0
35.8
1.1
7.9
15.8
6.3
55.3
63.2
71.1
61.6
PU-1
26.5
17.9
0.0
0.0
19.2
3.8
19.7
12.8
0.0
44.4
0.0
23.1
41.0
19.2
32.5
55.6
73.5
51.7
KRC2A
26.1
26.1
0.0
1.4
3.3
0.9
18.5
23.7
0.0
52.1
1.4
4.3
30.3
3.3
42.2
46.4
72.5
45.5
KRC2B
57.5
25.1
1.1
1.1
0.0
0.0
14.0
0.6
0.6
82.7
2.2
0.6
25.7
0.6
14.5
15.1
40.2
15.1
KRC4
3.5
15.3
0.6
1.8
0.0
0.0
41.2
37.6
0.0
18.8
2.4
0.0
15.3
0.0
78.8
78.8
94.1
78.8
KRC5
8.8
24.2
0.0
0.4
0.0
0.9
37.9
27.8
0.0
33.0
0.4
0.9
25.1
0.0
65.6
66.5
90.7
65.6
BEN2
32.4
27.8
0.0
0.0
4.6
0.0
20.4
14.8
0.0
60.2
0.0
4.6
32.4
4.6
35.2
39.8
67.6
39.8
BEN5A
6.4
16.5
0.0
0.0
0.0
1.6
48.9
26.6
0.0
22.9
0.0
1.6
18.1
0.0
75.5
77.1
93.6
75.5
BEN5B
55.4
19.1
0.6
0.6
0.0
1.3
22.9
0.0
0.0
74.5
1.3
1.3
20.4
0.0
22.9
24.2
43.3
22.9
Table S1: Modal composition data from the analysed sandstones. Q
m
= monocrystalline qartz; Q
p
= polycrystalline quartz; P = plagioclase;
K = potassium feldspar; L
met
= metamorphic clasts; L
v
= volcanic clasts; L
lim
= limestone clasts; D = dolomite clasts; L
p
= clasts of non-carbonate
sedimentary rocks; total of quartzose grains Q
t
= Q
m
+ Q
p
; total of feldspar F = P + K; total of lithic clasts L
t
= Q
p
+ L
met
+ L
v
+ L
p
; L = L
met
+ L
v
+ L
p
;
L
s
= L
met
+ L
p
; total of carbonate clasts L
carb
= L
lim
+ D; total of lithic clasts + carbonate clasts = L + Lc
arb
; L
t
+ L
carb
; L
s
+ L
carb
.
Supplement
ii
MADZIN, PLAŠIENKA and MÉRES
GEOLOGICA CARPATHICA
, 2019, 70, 1, 15–34
Formation
JPF
Sample
PU-5
Analysis
Tur#1
Tur#2
Tur#3
Tur#4
Tur#5
Tur#6
Tur#7
Tur#8
Tur#9
Tur#10
Tur#11
Tur#12
Tur#13
Tur#14
SiO
2
36.71
36.59
36.49
36.67
36.94
36.19
36.26
37.56
36.81
36.95
36.01
36.85
36.45
36.61
TiO
2
0.51
0.77
0.76
0.92
0.83
0.65
0.85
0.17
0.11
0.84
0.35
0.56
0.51
0.31
B
2
O
3
*
10.66
10.70
10.60
10.67
10.80
10.66
10.55
10.92
10.65
10.67
10.38
10.74
10.82
10.54
Al
2
O
3
32.32
32.29
31.35
31.35
33.18
34.80
31.40
35.00
30.26
31.09
28.16
32.95
35.92
30.92
Cr
2
O
3
0.04
0.05
0.06
0.06
0.07
0.00
0.00
0.06
0.00
0.01
0.00
0.06
0.00
0.01
V
2
O
3
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
Fe
2
O
3
*
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
1.62
0.00
2.80
0.00
0.00
0.00
FeO
9.55
6.68
9.42
7.18
7.40
10.73
9.78
5.22
8.41
8.06
8.79
7.55
8.19
8.43
MnO
0.01
0.01
0.00
0.02
0.03
0.08
0.04
0.01
0.01
0.01
0.02
0.03
0.07
0.01
MgO
5.54
7.27
6.00
7.45
6.35
2.86
5.65
6.93
7.43
7.10
7.11
6.44
4.31
6.98
NiO
0.00
0.02
0.01
0.02
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.05
0.01
0.00
ZnO
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
CaO
0.34
0.68
0.51
0.99
0.73
0.20
0.37
0.21
0.02
0.40
0.07
0.29
0.22
0.36
Na
2
O
2.37
2.25
2.51
2.09
1.93
1.90
2.43
1.66
2.91
2.58
2.76
2.28
1.80
2.44
K
2
O
0.02
0.02
0.02
0.01
0.01
0.04
0.02
0.02
0.03
0.02
0.04
0.01
0.05
0.01
H
2
O*
3.41
3.37
3.36
3.38
3.34
3.18
3.39
3.51
3.67
3.42
3.58
3.44
3.29
3.53
F
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
Cl
0.01
0.01
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.04
0.01
Total
101.47
100.70
101.09
100.83
101.60
101.30
100.76
101.28
101.93
101.16
100.09
101.24
101.67
100.14
Si
4+
5.98
5.94
5.98
5.97
5.95
5.90
5.97
5.98
6.01
6.02
6.03
5.96
5.86
6.04
Al
3+
0.02
0.06
0.02
0.03
0.05
0.10
0.03
0.02
0.00
0.00
0.00
0.04
0.14
0.00
T-sum.
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.01
6.02
6.03
6.00
6.00
6.04
B
3+
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
Al
3+
5.94
5.88
5.90
5.82
5.86
5.96
5.93
5.96
5.82
5.93
5.56
5.94
5.96
5.94
Cr
3+
0.00
0.01
0.01
0.01
0.01
0.00
0.00
0.01
0.00
0.00
0.00
0.01
0.00
0.00
V
3+
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
Mg
2+
0.06
0.12
0.09
0.17
0.13
0.03
0.07
0.04
0.00
0.07
0.01
0.05
0.04
0.06
Fe
3+
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.17
0.00
0.43
0.00
0.00
0.00
Z-sum.
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
Ti
4+
0.06
0.09
0.09
0.11
0.10
0.08
0.11
0.02
0.01
0.10
0.04
0.07
0.06
0.04
Al
3+
0.26
0.25
0.14
0.17
0.38
0.62
0.14
0.59
0.00
0.04
0.00
0.31
0.69
0.07
Fe
3+
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.03
0.00
0.00
0.00
0.00
0.00
Fe
2+
1.30
0.91
1.29
0.98
1.00
1.46
1.35
0.70
1.15
1.10
1.16
1.02
1.10
1.16
Mn
2+
0.00
0.00
0.00
0.00
0.00
0.01
0.01
0.00
0.00
0.00
0.00
0.00
0.01
0.00
Mg
2+
1.29
1.64
1.38
1.64
1.40
0.66
1.32
1.61
1.80
1.65
1.76
1.50
0.99
1.65
Zn
2+
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
Ni
2+
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.00
Vac.
0.09
0.11
0.10
0.10
0.13
0.16
0.08
0.08
0.01
0.11
0.03
0.09
0.14
0.07
Y-sum.
2.91
2.89
2.90
2.90
2.87
2.84
2.92
2.92
2.99
2.89
2.97
2.91
2.86
2.93
Ca
2+
0.06
0.12
0.09
0.17
0.13
0.03
0.07
0.04
0.00
0.07
0.01
0.05
0.04
0.06
Na
+
0.75
0.71
0.80
0.66
0.60
0.60
0.78
0.51
0.92
0.81
0.90
0.71
0.56
0.78
K
+
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.01
0.00
0.01
0.00
0.01
0.00
Vac.
0.19
0.17
0.11
0.17
0.27
0.36
0.15
0.45
0.07
0.11
0.08
0.23
0.39
0.15
X-sum.
0.81
0.83
0.89
0.83
0.73
0.64
0.85
0.55
0.93
0.89
0.92
0.77
0.61
0.85
F
-
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
Cl
-
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
OH
-
3.71
3.65
3.67
3.67
3.58
3.46
3.73
3.73
4.00
3.72
4.00
3.71
3.53
3.88
O
2-
0.29
0.35
0.33
0.33
0.42
0.54
0.27
0.27
0.00
0.28
0.00
0.29
0.46
0.11
V+W
sum.
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
Cat.
sum.
18.72
18.73
18.79
18.73
18.60
18.48
18.76
18.47
18.93
18.80
18.92
18.68
18.47
18.81
Al
sum.
6.21
6.18
6.06
6.02
6.30
6.69
6.10
6.57
5.82
5.97
5.56
6.29
6.80
6.01
Table S2: Microprobe analyses of detrital tourmalines from the sediments studied.
iii
PROVENANCE OF SYNOROGENIC DEPOSITS OF THE JARMUTA–PROČ FORMATION
GEOLOGICA CARPATHICA
, 2019, 70, 1, 15–34
Table S2 (continued):
Formation
JPF
MB
JPF
Sample
PU-5
SZTOL-1
LIT-1
H-15
Analysis
Tur#15 Tur#16 Tur#17 Tur#18 Tur#19 Tur#20 Tur#21 Tur#22 Tur#23 Tur#24 Tur#25 Tur#26 Tur#27 Tur#28 Tur#29
SiO
2
36.51
36.49
36.24
37.00
35.21
36.91
36.66
36.19
36.05
35.05
34.82
36.73
37.51
36.73
37.29
TiO
2
1.05
0.85
1.34
0.48
0.78
1.18
0.59
0.76
0.69
1.08
1.14
0.78
0.86
1.02
0.60
B
2
O
3
*
10.51
10.54
10.53
10.76
10.50
10.75
10.53
10.47
10.42
10.41
10.22
10.81
10.82
10.83
10.90
Al
2
O
3
30.14
30.56
30.20
33.18
33.33
31.49
28.21
27.10
28.48
32.15
30.46
32.90
31.37
33.01
33.20
Cr
2
O
3
0.16
0.04
0.00
0.02
0.00
0.14
0.00
0.01
0.01
0.05
0.03
0.00
0.09
0.09
0.02
V
2
O
3
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
Fe
2
O
3
*
0.00
0.00
0.00
0.00
0.00
0.00
2.44
4.56
1.81
0.00
0.00
0.00
0.00
0.00
0.00
FeO
10.56
10.23
11.18
9.18
13.29
7.53
9.08
8.76
12.27
8.01
8.45
5.53
5.49
5.72
5.83
MnO
0.01
0.01
0.03
0.01
0.10
0.01
0.00
0.00
0.05
0.07
0.03
0.00
0.00
0.00
0.00
MgO
5.60
5.88
5.48
5.59
2.64
7.22
7.44
7.33
5.43
5.78
6.13
7.93
8.80
7.68
7.69
NiO
0.05
0.00
0.00
0.02
0.01
0.00
0.00
0.00
0.03
0.01
0.02
0.00
0.00
0.00
0.00
ZnO
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
CaO
0.30
0.32
0.46
0.15
0.48
1.01
0.06
0.05
0.06
0.81
0.35
0.85
0.41
0.95
0.75
Na
2
O
2.66
2.62
2.57
2.13
1.91
2.04
2.90
2.78
2.90
1.90
2.32
2.24
2.58
2.01
2.28
K
2
O
0.02
0.02
0.02
0.02
0.03
0.02
0.06
0.07
0.06
0.03
0.01
0.04
0.03
0.04
0.03
H
2
O*
3.35
3.42
3.40
3.54
3.42
3.35
3.63
3.61
3.59
3.27
3.34
3.37
3.49
3.35
3.36
F
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
Cl
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
Total
100.93
100.97
101.46
102.10
101.70
101.66
101.61
101.70
101.84
98.63
97.33
101.20
101.45
101.45
101.96
Si
4+
6.04
6.02
5.98
5.98
5.83
5.97
6.05
6.01
6.01
5.85
5.92
5.91
6.02
5.89
5.95
Al
3+
0.00
0.00
0.02
0.02
0.17
0.03
0.00
0.00
0.00
0.15
0.08
0.09
0.00
0.11
0.05
T-sum.
6.04
6.02
6.00
6.00
6.00
6.00
6.05
6.01
6.01
6.00
6.00
6.00
6.02
6.00
6.00
B
3+
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
Al
3+
5.87
5.94
5.86
5.97
5.92
5.81
5.49
5.30
5.60
5.85
5.93
5.85
5.92
5.82
5.87
Cr
3+
0.02
0.01
0.00
0.00
0.00
0.02
0.00
0.00
0.00
0.01
0.00
0.00
0.01
0.01
0.00
V
3+
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
Mg
2+
0.05
0.06
0.08
0.03
0.08
0.18
0.01
0.01
0.01
0.14
0.06
0.15
0.07
0.16
0.13
Fe
3+
0.05
0.00
0.06
0.00
0.00
0.00
0.50
0.69
0.39
0.00
0.00
0.00
0.00
0.00
0.00
Z-sum.
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
Ti
4+
0.13
0.11
0.17
0.06
0.10
0.14
0.07
0.09
0.09
0.14
0.15
0.09
0.10
0.12
0.07
Al
3+
0.00
0.00
0.00
0.32
0.41
0.16
0.00
0.00
0.00
0.33
0.09
0.29
0.02
0.31
0.32
Fe
3+
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
Fe
2+
1.41
1.41
1.48
1.24
1.84
1.02
1.06
1.10
1.55
1.12
1.20
0.74
0.74
0.77
0.78
Mn
2+
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.01
0.01
0.00
0.00
0.00
0.00
0.00
Mg
2+
1.33
1.39
1.27
1.32
0.57
1.56
1.82
1.80
1.34
1.30
1.49
1.76
2.04
1.67
1.70
Zn
2+
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
Ni
2+
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
Vac.
0.13
0.09
0.08
0.06
0.07
0.12
0.05
0.01
0.01
0.11
0.07
0.12
0.10
0.12
0.13
Y-sum.
2.87
2.91
2.92
2.94
2.93
2.88
2.95
2.99
2.99
2.89
2.93
2.88
2.90
2.88
2.87
Ca
2+
0.05
0.06
0.08
0.03
0.08
0.18
0.01
0.01
0.01
0.14
0.06
0.15
0.07
0.16
0.13
Na
+
0.85
0.84
0.82
0.67
0.61
0.64
0.93
0.89
0.94
0.62
0.77
0.70
0.80
0.63
0.71
K
+
0.00
0.00
0.00
0.00
0.01
0.00
0.01
0.01
0.01
0.01
0.00
0.01
0.01
0.01
0.01
Vac.
0.09
0.10
0.09
0.30
0.30
0.18
0.05
0.08
0.04
0.23
0.17
0.15
0.12
0.20
0.16
X-sum.
0.91
0.90
0.91
0.70
0.70
0.82
0.95
0.92
0.96
0.77
0.83
0.85
0.88
0.80
0.84
F
-
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
Cl
-
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
OH
-
3.69
3.76
3.74
3.82
3.77
3.62
4.00
4.00
4.00
3.64
3.78
3.61
3.74
3.59
3.58
O
2-
0.31
0.24
0.26
0.18
0.23
0.38
0.00
0.00
0.00
0.36
0.22
0.39
0.26
0.41
0.42
V+W
sum.
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
Cat.
sum.
18.82
18.83
18.83
18.64
18.63
18.70
18.95
18.92
18.96
18.66
18.77
18.73
18.80
18.67
18.71
Al
sum.
5.87
5.94
5.87
6.32
6.50
6.00
5.49
5.30
5.60
6.33
6.10
6.24
5.94
6.24
6.24
iv
MADZIN, PLAŠIENKA and MÉRES
GEOLOGICA CARPATHICA
, 2019, 70, 1, 15–34
Table S2 (continued):
Formation
MB
JPF
JPF
Sample
MIL-2
DRAB-3
KRC-5
Analysis
Tur#30 Tur#31 Tur#32 Tur#43 Tur#43 Tur#43 Tur#36 Tur#37 Tur#38 Tur#39 Tur#40 Tur#41 Tur#42 Tur#43 Tur#44 Tur#45
SiO
2
37.40
36.16
34.71
36.32
36.32
36.32
36.80
37.44
37.19
36.86
36.39
35.65
35.76
36.32
35.81
35.84
TiO
2
0.24
0.30
4.37
0.82
0.82
0.82
0.75
1.07
0.27
1.36
0.79
0.86
0.68
0.82
0.46
0.12
B
2
O
3
*
10.88
10.53
10.27
10.68
10.68
10.68
10.69
10.79
10.93
10.63
10.51
10.65
10.56
10.68
10.48
10.31
Al
2
O
3
34.16
31.21
26.50
33.71
33.71
33.71
31.69
31.53
35.07
30.29
29.18
33.98
33.74
33.71
33.31
27.55
Cr
2
O
3
0.05
0.03
0.02
0.11
0.11
0.11
0.03
0.04
0.03
0.04
0.00
0.12
0.03
0.11
0.01
0.04
V
2
O
3
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
Fe
2
O
3
*
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
1.42
0.00
0.00
0.00
0.00
2.91
FeO
5.95
9.41
11.97
5.92
5.92
5.92
7.15
7.60
5.87
8.01
6.88
5.51
9.33
5.92
11.24
8.41
MnO
0.01
0.06
0.09
0.00
0.00
0.00
0.03
0.02
0.05
0.05
0.04
0.00
0.06
0.00
0.06
0.01
MgO
7.13
6.50
5.71
6.47
6.47
6.47
7.39
7.16
6.56
7.31
8.34
6.70
4.44
6.47
3.24
7.61
NiO
0.00
0.00
0.01
0.00
0.00
0.00
0.02
0.00
0.01
0.01
0.00
0.00
0.04
0.00
0.01
0.00
ZnO
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
CaO
0.28
0.18
1.00
0.20
0.20
0.20
0.64
0.20
0.50
0.54
0.00
1.03
0.54
0.20
0.79
0.41
Na
2
O
1.89
2.75
2.24
2.24
2.24
2.24
2.21
2.59
2.00
2.28
2.76
1.62
1.57
2.24
1.36
2.71
K
2
O
0.01
0.01
0.08
0.02
0.02
0.02
0.01
0.02
0.03
0.02
0.04
0.03
0.03
0.02
0.02
0.04
H
2
O*
3.55
3.59
3.16
3.27
3.27
3.27
3.46
3.42
3.36
3.44
3.62
3.25
3.36
3.27
3.26
3.56
F
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
Cl
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.01
0.00
0.00
0.02
0.00
Total
101.56
100.72
100.13
99.76
99.76
99.76
100.86
101.89
101.86
100.83
99.98
99.42
100.13
99.76
100.07
99.52
Si
4+
5.97
5.97
5.87
5.91
5.91
5.91
5.98
6.03
5.92
6.03
6.02
5.82
5.89
5.91
5.94
6.04
Al
3+
0.03
0.03
0.13
0.09
0.09
0.09
0.02
0.00
0.08
0.00
0.00
0.18
0.11
0.09
0.06
0.00
T-sum.
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.03
6.00
6.03
6.02
6.00
6.00
6.00
6.00
6.04
B
3+
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
Al
3+
5.95
5.96
5.16
5.95
5.95
5.95
5.89
5.96
5.91
5.84
5.69
5.80
5.90
5.95
5.86
5.47
Cr
3+
0.01
0.00
0.00
0.01
0.01
0.01
0.00
0.01
0.00
0.01
0.00
0.02
0.00
0.01
0.00
0.01
V
3+
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
Mg
2+
0.05
0.03
0.18
0.03
0.03
0.03
0.11
0.03
0.08
0.09
0.00
0.18
0.10
0.03
0.14
0.07
Fe
3+
0.00
0.00
0.66
0.00
0.00
0.00
0.00
0.00
0.00
0.06
0.31
0.00
0.00
0.00
0.00
0.45
Z-sum.
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
Ti
4+
0.03
0.04
0.56
0.10
0.10
0.10
0.09
0.13
0.03
0.17
0.10
0.11
0.08
0.10
0.06
0.01
Al
3+
0.46
0.07
0.00
0.42
0.42
0.42
0.17
0.03
0.58
0.00
0.00
0.55
0.53
0.42
0.60
0.00
Fe
3+
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
Fe
2+
0.79
1.30
1.04
0.81
0.81
0.81
0.97
1.02
0.78
1.03
0.82
0.75
1.28
0.81
1.56
1.11
Mn
2+
0.00
0.01
0.01
0.00
0.00
0.00
0.00
0.00
0.01
0.01
0.01
0.00
0.01
0.00
0.01
0.00
Mg
2+
1.65
1.57
1.26
1.53
1.53
1.53
1.68
1.69
1.47
1.69
2.06
1.45
0.99
1.53
0.66
1.84
Zn
2+
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
Ni
2+
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
Vac.
0.07
0.01
0.13
0.14
0.14
0.14
0.08
0.13
0.13
0.10
0.02
0.14
0.09
0.14
0.12
0.04
Y-sum.
2.93
2.99
2.87
2.86
2.86
2.86
2.92
2.87
2.87
2.90
2.98
2.86
2.91
2.86
2.88
2.96
Ca
2+
0.05
0.03
0.18
0.03
0.03
0.03
0.11
0.03
0.08
0.09
0.00
0.18
0.10
0.03
0.14
0.07
Na
+
0.59
0.88
0.73
0.71
0.71
0.71
0.70
0.81
0.62
0.72
0.88
0.51
0.50
0.71
0.44
0.89
K
+
0.00
0.00
0.02
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.01
0.01
0.01
0.00
0.00
0.01
Vac.
0.36
0.09
0.07
0.26
0.26
0.26
0.19
0.15
0.29
0.18
0.11
0.30
0.40
0.26
0.42
0.03
X-sum.
0.64
0.91
0.93
0.74
0.74
0.74
0.81
0.85
0.71
0.82
0.89
0.70
0.60
0.74
0.58
0.97
F
-
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
Cl
-
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
OH
-
3.79
3.95
3.57
3.55
3.55
3.55
3.75
3.67
3.57
3.75
4.00
3.54
3.69
3.55
3.61
4.00
O
2-
0.21
0.05
0.43
0.45
0.45
0.45
0.25
0.33
0.43
0.25
0.00
0.46
0.31
0.45
0.39
0.00
V+W
sum.
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
Cat.
sum.
18.57
18.90
18.80
18.61
18.61
18.61
18.73
18.75
18.57
18.75
18.89
18.56
18.51
18.61
18.47
18.97
Al
sum.
6.43
6.07
5.29
6.46
6.46
6.46
6.07
5.99
6.57
5.84
5.69
6.54
6.54
6.46
6.51
5.47
v
PROVENANCE OF SYNOROGENIC DEPOSITS OF THE JARMUTA–PROČ FORMATION
GEOLOGICA CARPATHICA
, 2019, 70, 1, 15–34
Formation
JPF
JPF
Sample
PU-5
SZTOL-1
Analysis
Grt#1
Grt#2
Grt#3
Grt#4
Grt#5
Grt#6
Grt#7
Grt#8
Grt#9
Grt#10
Grt#11
Grt#12
SiO
2
35.80
36.71
36.89
36.82
37.22
37.31
37.16
37.17
37.53
36.75
37.26
37.31
TiO
2
0.08
0.12
0.05
0.10
0.14
0.09
0.07
0.13
0.07
0.11
0.13
0.09
Al
2
O
3
20.93
21.01
21.17
21.01
21.07
21.41
21.10
21.01
21.43
21.33
21.33
21.56
FeO
29.21
29.17
37.00
35.37
28.50
25.53
27.70
26.09
33.30
34.19
31.81
32.60
MnO
10.71
8.80
2.23
2.20
3.25
11.65
9.12
6.68
0.28
5.64
6.74
4.10
MgO
1.62
1.07
1.62
1.58
0.77
2.16
0.93
0.81
1.57
1.02
1.01
1.20
CaO
1.73
3.78
2.06
3.10
9.60
3.06
3.92
8.45
6.68
2.92
3.89
5.20
Cr
2
O
3
0.07
0.02
0.00
0.00
0.01
0.06
0.02
0.01
0.03
0.04
0.02
0.02
Total
100.14
100.67
101.01
100.19
100.55
101.27
100.02
100.35
100.89
101.99
102.20
102.08
Formula normalization to 12 oxydes and 8 cations
Si
2.926
2.969
2.975
2.984
2.976
2.977
3.001
2.983
2.987
2.949
2.970
2.964
Al
IV
0.074
0.031
0.025
0.016
0.024
0.023
0.000
0.017
0.013
0.051
0.030
0.036
Al
VI
1.946
1.973
1.989
1.991
1.964
1.990
2.014
1.971
1.999
1.967
1.975
1.984
Ti
0.005
0.007
0.003
0.006
0.008
0.006
0.004
0.008
0.004
0.006
0.008
0.006
Cr
0.004
0.001
0.000
0.000
0.001
0.004
0.001
0.001
0.002
0.002
0.001
0.001
Fe
3+
0.040
0.016
0.007
0.003
0.024
0.000
0.000
0.018
0.000
0.021
0.014
0.008
Fe
2+
1.956
1.957
2.488
2.395
1.882
1.703
1.898
1.733
2.223
2.273
2.107
2.158
Mn
0.742
0.603
0.152
0.151
0.220
0.787
0.624
0.454
0.019
0.383
0.455
0.276
Mg
0.198
0.129
0.194
0.191
0.091
0.257
0.112
0.096
0.187
0.122
0.121
0.142
Ca
0.152
0.327
0.178
0.270
0.822
0.262
0.340
0.726
0.569
0.251
0.333
0.442
Grt end members (mol. %)
almandine
62.7
64.3
82.4
79.5
61.9
56.1
63.8
57.2
74.1
74.4
69.4
71.0
pyrope
6.8
4.3
6.5
6.4
3.1
8.6
3.8
3.2
6.2
4.1
4.1
4.8
grossular
2.9
10.2
5.6
8.9
26.4
8.6
11.4
23.4
19.0
7.3
10.4
14.4
spessartine
25.4
20.3
5.1
5.1
7.4
26.4
21.0
15.2
0.6
13.0
15.3
9.3
uvarovite
0.2
0.1
0.0
0.0
0.0
0.2
0.1
0.0
0.1
0.1
0.1
0.1
andradite
2.1
0.8
0.4
0.1
1.2
0.0
0.0
0.9
0.0
1.1
0.7
0.4
Formation
JPF
MB
JPF
MB
Sample
SZTOL-1
LIT-1
H-15
MIL-2
Analysis
Grt#13
Grt#14
Grt#15
Grt#16
Grt#17
Grt#18
Grt#19
Grt#20
Grt#21
Grt#22
Grt#23
SiO
2
37.38
37.01
37.24
36.07
34.52
35.11
36.98
37.45
37.10
36.43
36.88
TiO
2
0.03
0.05
0.09
0.00
0.05
0.07
0.07
0.08
0.03
0.05
0.05
Al
2
O
3
21.35
21.43
21.44
21.22
20.66
20.89
21.12
21.25
21.53
21.22
21.52
FeO
35.80
31.80
27.41
32.65
22.54
33.79
34.18
35.56
32.45
35.36
34.87
MnO
1.55
5.47
8.15
6.21
20.49
3.80
4.56
4.20
6.19
3.87
2.94
MgO
2.57
0.84
0.67
3.01
0.56
3.23
1.31
1.49
3.28
1.48
1.40
CaO
2.98
5.21
7.08
1.09
0.45
1.54
3.62
2.32
1.28
1.96
3.14
Cr
2
O
3
0.00
0.03
0.04
0.00
0.00
0.08
0.00
0.00
0.03
0.00
0.01
Total
101.67
101.84
102.12
100.25
99.28
98.51
101.84
102.33
101.88
100.36
100.82
Formula normalization to 12 oxydes and 8 cations
Si
2.971
2.957
2.957
2.922
2.886
2.893
2.960
2.983
2.945
2.961
2.966
Al
IV
0.029
0.043
0.043
0.078
0.114
0.107
0.040
0.017
0.055
0.039
0.034
Al
VI
1.973
1.977
1.966
1.952
1.927
1.926
1.956
1.979
1.962
1.995
2.009
Ti
0.002
0.003
0.006
0.000
0.003
0.004
0.004
0.004
0.002
0.003
0.003
Cr
0.000
0.002
0.002
0.000
0.000
0.005
0.000
0.000
0.002
0.000
0.001
Fe
3+
0.022
0.016
0.024
0.043
0.062
0.057
0.035
0.015
0.031
0.002
0.000
Fe
2+
2.358
2.109
1.797
2.169
1.514
2.271
2.253
2.353
2.123
2.402
2.362
Mn
0.105
0.370
0.548
0.426
1.451
0.265
0.309
0.283
0.416
0.266
0.200
Mg
0.305
0.100
0.079
0.364
0.070
0.397
0.156
0.176
0.388
0.179
0.168
Ca
0.254
0.446
0.602
0.094
0.040
0.136
0.310
0.198
0.108
0.171
0.271
Grt end members (mol. %)
almandine
77.7
69.0
58.4
69.8
45.9
72.4
73.8
78.0
69.0
79.2
78.5
pyrope
10.3
3.4
2.7
12.5
2.4
13.7
5.3
5.9
13.2
6.1
5.7
grossular
7.4
14.2
19.0
1.0
0.0
1.5
8.7
5.9
2.0
5.7
9.1
spessartine
3.5
12.5
18.5
14.6
50.3
9.2
10.4
9.5
14.1
9.0
6.8
uvarovite
0.0
0.1
0.1
0.0
0.0
0.3
0.0
0.0
0.1
0.0
0.0
andradite
1.1
0.8
1.2
2.2
1.4
3.0
1.8
0.8
1.6
0.1
0.0
Table S3: Microprobe analyses of detrital garnets from the sediments studied.
Table S3 (continued):
vi
MADZIN, PLAŠIENKA and MÉRES
GEOLOGICA CARPATHICA
, 2019, 70, 1, 15–34
Formation
JPF
JPF
Sample
KRC-5
BEN-5
Analysis
Grt#24
Grt#25
Grt#26
Grt#27
Grt#28
Grt#29
Grt#30
Grt#31
Grt#32
Grt#33
Grt#34
Grt#35
SiO
2
37.46
36.81
38.69
37.21
37.91
39.36
37.86
40.02
39.17
37.17
37.56
37.92
TiO
2
0.15
0.00
0.06
0.00
0.00
0.05
0.08
0.03
0.09
0.31
0.06
0.01
Al
2
O
3
21.49
21.44
22.56
21.66
21.90
22.47
21.38
23.05
22.44
20.72
21.45
21.86
FeO
25.43
33.27
27.15
33.94
30.87
21.30
26.41
20.61
23.25
17.72
21.99
33.53
MnO
3.62
2.82
0.50
2.37
1.45
0.47
0.57
0.48
0.84
16.33
10.91
1.38
MgO
3.31
3.98
10.17
4.34
6.76
8.03
6.23
9.89
6.64
0.93
1.51
5.48
CaO
8.61
1.27
1.30
1.43
1.54
9.22
7.49
7.27
8.96
8.26
7.07
1.38
Cr
2
O
3
0.01
0.02
0.02
0.00
0.02
0.00
0.04
0.01
0.00
0.05
0.03
0.00
Total
100.08
99.61
100.44
100.95
100.45
100.90
100.05
101.36
101.38
101.48
100.58
101.56
Formula normalization to 12 oxydes and 8 cations
Si
2.961
2.963
2.955
2.953
2.965
2.977
2.950
2.980
2.978
2.958
2.989
2.965
Al
IV
0.039
0.037
0.045
0.047
0.035
0.023
0.050
0.020
0.022
0.042
0.011
0.035
Al
VI
1.965
1.998
1.987
1.980
1.986
1.981
1.920
2.005
1.990
1.907
2.003
1.981
Ti
0.009
0.000
0.003
0.000
0.000
0.003
0.004
0.002
0.005
0.018
0.004
0.000
Cr
0.000
0.001
0.001
0.000
0.001
0.000
0.003
0.000
0.000
0.003
0.002
0.000
Fe
3+
0.022
0.001
0.008
0.018
0.012
0.014
0.065
0.000
0.005
0.064
0.000
0.016
Fe
2+
1.659
2.239
1.727
2.235
2.007
1.332
1.656
1.292
1.473
1.116
1.476
2.177
Mn
0.243
0.192
0.032
0.159
0.096
0.030
0.038
0.030
0.054
1.101
0.735
0.092
Mg
0.391
0.478
1.158
0.514
0.788
0.905
0.723
1.098
0.752
0.111
0.179
0.638
Ca
0.729
0.110
0.106
0.122
0.129
0.747
0.626
0.580
0.730
0.704
0.603
0.116
Grt end members (mol. %)
almandine
54.0
73.7
56.1
73.1
65.8
43.5
53.0
42.7
48.4
35.2
49.2
71.5
pyrope
13.2
16.1
39.2
17.4
26.6
30.4
24.5
36.9
25.3
3.7
6.0
21.5
grossular
23.5
3.6
3.2
3.2
3.7
24.4
17.8
19.4
24.3
20.4
20.1
3.1
spessartine
8.2
6.5
1.1
5.4
3.2
1.0
1.3
1.0
1.8
37.2
24.6
3.1
uvarovite
0.0
0.1
0.0
0.0
0.1
0.0
0.1
0.0
0.0
0.2
0.1
0.0
andradite
1.1
0.0
0.4
0.9
0.6
0.7
3.3
0.0
0.2
3.2
0.0
0.8
Formation
JPF
JPF
MB
JPF
JPF
JPF
Sample
PU-5
Sztol-1
LIT-1
H-15
DRAB-3
KRC-5
Analysis
Spl#1
Spl#2
Spl#3
Spl#4
Spl#5
Spl#6
Spl#7
Spl#8
Spl#10
Spl#11 Spl#12 Spl#13 Spl#14 Spl#15
Degree of alteration
U
U
I
U
I
I
U
U
II
U
U
U
U
U
SiO
2
0.09
0.02
0.00
0.01
0.03
0.04
0.03
0.01
0.00
0.01
0.01
0.00
0.04
0.01
TiO
2
0.31
0.05
0.30
0.05
0.02
0.08
0.10
0.09
3.26
0.08
0.04
0.08
0.06
0.04
V
2
O
5
0.12
0.24
0.23
0.12
0.31
0.04
0.16
0.07
0.36
0.25
0.22
0.21
0.22
0.19
Al
2
O
3
36.62
23.97
12.76
42.58
19.95
25.20
36.39
51.65
6.83
23.73
19.84
26.47
26.57
25.73
Cr
2
O
3
29.69
47.46
55.73
25.73
49.55
41.63
32.67
17.63
35.05
47.35
51.53
43.51
43.23
45.44
Fe
2
O
3
*
5.48
2.40
4.16
1.98
1.22
5.56
3.08
2.14
23.89
1.57
1.50
2.25
1.49
1.73
FeO
13.07
12.39
21.25
12.21
17.83
18.57
14.91
10.70
28.64
15.70
15.27
15.49
12.05
12.64
MnO
0.28
0.33
0.43
0.24
0.44
0.35
0.26
0.14
0.43
0.30
0.39
0.33
0.25
0.26
MgO
16.27
15.51
8.68
16.98
11.10
11.65
15.26
19.35
2.30
13.31
13.07
13.60
15.39
15.37
CoO
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
NiO
0.11
0.13
0.04
0.24
0.02
0.10
0.12
0.28
0.34
0.11
0.07
0.07
0.15
0.14
ZnO
0.08
0.05
0.28
0.21
0.12
0.26
0.12
0.17
0.26
0.12
0.11
0.23
0.10
0.05
Total
101.57
102.30
103.45
100.15
100.46
102.92
102.80
102.01
98.97
102.38
101.91
102.03
99.39
101.43
Based on 3 cations
Cr
0.660
1.106
1.406
0.564
1.226
0.984
0.725
0.364
0.981
1.120
1.244
1.019
1.022
1.060
Ti
0.007
0.001
0.007
0.001
0.001
0.002
0.002
0.002
0.087
0.002
0.001
0.002
0.001
0.001
V
0.002
0.005
0.005
0.002
0.006
0.001
0.003
0.001
0.008
0.005
0.004
0.004
0.004
0.004
Al
1.214
0.833
0.480
1.391
0.736
0.888
1.204
1.591
0.285
0.837
0.714
0.924
0.937
0.896
Fe
3+
0.108
0.048
0.089
0.038
0.023
0.123
0.061
0.039
0.543
0.029
0.030
0.045
0.029
0.034
Fe
2+
0.315
0.310
0.578
0.286
0.472
0.466
0.355
0.237
0.942
0.399
0.395
0.389
0.306
0.316
Mn
0.007
0.008
0.012
0.006
0.012
0.009
0.006
0.003
0.013
0.008
0.010
0.008
0.006
0.007
Mg
0.682
0.682
0.413
0.701
0.518
0.519
0.638
0.754
0.121
0.593
0.595
0.600
0.686
0.676
Co
0.000
0.000
0.000
0.000
0.000
0.000
0.000
0.000
0.000
0.000
0.000
0.000
0.000
0.000
Ni
0.003
0.003
0.001
0.005
0.000
0.002
0.003
0.006
0.010
0.003
0.002
0.002
0.004
0.003
Zn
0.002
0.001
0.007
0.004
0.003
0.006
0.002
0.003
0.007
0.003
0.002
0.005
0.002
0.001
Total
2.999
2.998
2.998
2.999
2.997
3.000
2.999
2.999
2.996
2.998
2.998
2.998
2.998
2.998
Cr#
35
57
75
29
62
53
38
19
77
57
64
52
52
54
Mg#
68
69
42
71
52
53
64
76
11
60
60
61
69
68
Fe
2+
/Fe
3+
2.9
6.4
6.5
7.5
20.6
3.8
5.9
6.1
1.7
13.6
13.2
8.7
10.6
9.2
Table S3 (continued):
Table S4: Microprobe analyses of detrital spinels from the sediments studied. * Fe
2
O
3
calculated from stoichiometry. Cr# = Cr / (Cr + Al);
Mg# = Mg / (Mg + Fe
2+
). Criteria for alteration degrees according to Mikuš &Spišiak (2007); U — unaltered fresh spinel.