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, OCTOBER 2014, 65, 5, 329—338 doi: 10.2478/geoca-2014-0023
Provenance of Permian Malužiná Formation sandstones
(Hronicum, Western Carpathians): evidence from monazite
geochronology
ANNA VOZÁROVÁ
1
, PATRIK KONEČNÝ
2
, MAREK VĎAČNÝ
3
, JOZEF VOZÁR
4
and
KATARÍNA ŠARINOVÁ
1
1
Department of Mineralogy and Petrology, Faculty of Natural Sciences, Comenius University in Bratislava, Mlynská dolina G,
842 15 Bratislava, Slovak Republic; vozarova@fns.uniba.sk; sarinova@fns.uniba.sk
2
State Geological Institute of Dionýz Štúr, Mlynská dolina 1, 817 04 Bratislava, Slovak Republic; konecny.patrik@geology.sk
3
Geological Institute, Slovak Academy of Sciences; Branch: Ďumbierska 1, 974 01 Banská Bystrica, Slovak Republic; vdacny@savbb.sk
4
Geological Institute, Slovak Academy of Sciences, Dúbravská cesta 9, P.O. Box 106, 840 05 Bratislava, Slovak Republic;
jozef.vozar@savba.sk
(Manuscript received March 10, 2014; accepted in revised form October 7, 2014)
Abstract: The Permian Malužiná Formation and the Pennsylvanian Nižná Boca Formation are Upper Paleozoic vol-
cano-sedimentary complexes in the Hronicum nappe system. Sandstones, shales and conglomerates are the dominant
lithological members of the Malužiná Formation sequence. Detrital monazites were analysed by electron microprobe, to
obtain Th-U-Pb ages of the source areas. The majority of detrital monazites showed Devonian-Mississippian ages,
ranging from 330 to 380 Ma with a weighted average of 351 ± 3.3 (2
σ), that correspond well with the main phase of arc-
related magmatic activity in the Western Carpathians. Only a small portion of detrital monazites displayed Permian
ages in the range of 250—280 Ma, with a significant maximum around 255 Ma. The weighted average corresponds to
255 ± 6.2 Ma. These monazites may have been partially derived from the synsedimentary acid volcanism that was situ-
ated on the margins of the original depositional basin. However, some of the Triassic ages (230—240 Ma), reflect, most
likely, the genetic relationship with the overheating connected with Permian and subsequent Triassic extensional re-
gime. Detrital monazite ages document the Variscan age of the source area and also reflect a gradual development of the
Hronicum terrestrial rift, accompanied by the heterogeneous cooling of the lithosphere.
Key words: electron microprobe monazite dating, provenance, Permian sandstones, Hronicum, Western Carpathians.
Introduction
Detrital monazite is a common component of siliciclastic
sediments and sedimentary rocks, where it is concentrated in
heavy mineral assemblages. Monazite is generally stable
during sedimentary and diagenetic processes (Morton &
Hallsworth 1999), although alteration by the low-tempera-
ture brines associated with uranium mineralization has also
been reported (Mathieu et al. 2001). Detrital monazites are
believed to be unstable in the early stage of regional meta-
morphism, however, the relics of detrital monazite grains
have been reported from greenschist facies (e.g. Rubato et al.
2001; Wing et al. 2003; Rasmussen & Muhling 2009) and
even in amphibolite facies rock complexes (e.g. Williams
2001; Krenn et al. 2008). Therefore, chemical electron mi-
croprobe dating of detrital monazite also has a great poten-
tial to obtain reliable constraints useful for dating source
areas and further characteristics of provenance.
The present study reports the first detrital monazite ages
from the Permian sandstones of the Hronicum Unit, obtained
from the six samples cropping out in the Malé Karpaty Mts.
The aim of this study is to contribute to a better understand-
ing of the link between source areas of the Permian Hroni-
cum sedimentary rocks, as well as the tectono-metamorphic
evolution of the Western Carpathian Variscan mobile belt.
Geological setting
The Late Paleozoic volcanic and sedimentary rocks repre-
sented by the Ipoltica Group form the basal part of the multi-
nappe Hronicum Unit in the whole area of the Western
Carpathians. This Upper Paleozoic volcano-sedimentary se-
quence is distributed in almost all Western Carpathians
mountain ranges. Specifically, it occurs in the Malé Karpaty
Mts, in the central part of Slovakia, in the Nízke Tatry Mts
and Kozie chrbty hills (dominant distribution), in the base-
ment of the Tertiary of the Popradská and Hornádska kotlina
Depressions, as well as in the Levočské vrchy hills, the
Branisko Mts (fragmentary occurrences), and in the area of
the tectonic contact of the Gemericum and Veporicum Units
in the Čierna Hora Mts. On the basis of the most completely
preserved sedimentary successions on the northern slopes of
the Nízke Tatry Mts, the Ipoltica Group was defined as
the lithostratigraphic unit composed of two formations – the
Nižná Boca (Pennsylvanian) and the Malužiná (Permian)
Formations (Vozárová & Vozár 1981).
In the Malé Karpaty Mts, the rock complexes of the Ipoltica
Group emerge in the basal part of the lower (Šturec) nappe of
the Hronicum. Their occurrences extend in a wide belt (1.5—
2.5 km), from the villages of Smolenice and Lošonec in the
NE to the area that is S of Sološnica in the W (Fig. 1). The
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Mesozoic sequences of the Vysoká Nappe of the Fatricum
Unit form tectonic basement of the Hronicum in the whole
area of the Ipoltica Group. Both cover nappe units, the Hroni-
cum and Fatricum, have been transported over the underlying
Tatricum Unit during the Middle Cretaceous detachment and
nappe stacking. The possible emplacement mechanism was
studied by Prokešová et al. (2012 and references therein). Basal
parts of the Hronicum Unit, represented especially by the
Nižná Boca Formation (NBF), are markedly tectonically re-
duced in the Malé Karpaty Mts. Due to this, only the sedi-
ments of the Malužiná Formation (MF) were researched in the
present study. The MF mineralogical immature sediments ex-
amined are covered by the Lower Triassic quartzose sandstones.
Lithology
: The MF sediments are formed by a relatively mo-
notonous, markedly cyclically arranged, varicoloured com-
plex of siliciclastic sediments that are genetically associated
with a continental alluvial-lacustrine system deposited in arid/
semiarid climatic conditions. In the studied area, varicoloured
sandstones prevail and are associated with shales and fine-
grained conglomerates. Mineral composition of the sandstones
corresponds to subarkoses, arkoses and arkosic greywackes,
depending upon the type of sedimentary environment in which
they occur. Channel facies are structurally more mature, com-
posed of orthoconglomerates and sandstones with the grain-
supported fabric. These sandstones can be classified as arkoses
and less frequently as subarkoses, either with siliceous or calcif-
erous cement. The carbonate cement signalizes periods of more
intensive aridization of the climate. River-floodplain facies are
represented by structurally immature red arkosic greywackes,
with a higher content of the primary matrix. The MF is char-
acterized by the presence of basalts and basaltic andesites of
a continental tholeiite type, which are delimited into two erup-
tion phases in the Nízke Tatry Mts (Vozár 1977, 1997; Dostal
et al. 2003). In the area of the MF in the Malé Karpaty Mts, be-
sides the characteristic red-beds sediments, only the continental
tholeiites of the second volcanic eruption phase are preserved.
Sample characteristics
Detrital monazites were studied in six sandstone samples
(Fig. 1; Table 1). They have a low content of primary matrix,
Fig. 1. Map of Slovakia showing the location of the study area (marked by a rectangle). Details of the studied area are depicted below the map
of Slovakia in a form of a simplified geological map of the Late Paleozoic rocks of the Hronic Unit in the Malé Karpaty Mts (after
Vozárová & Vozár 1988). This geological map also shows five sampling sites. 1 – Quaternary sediments, 2 – Tertiary sediments. Hronic
Unit—Šturec Nappe: 3 – Middle and Upper Triassic – carbonates, undivided; 4 – Lower Triassic – quartz sandstones, shales; 5 – Per-
mian – andesites, basalts and volcanoclastics (Malužiná Formation); 6 – Permian – conglomerates, sandstones, shales with volcanogenic
material admixture (Malužiná Formation); 7 – Uppermost Pennsylvanian – grey conglomerates, sandstones, shales (Nižná Boca Formation).
Krížna Nappe: 8 – Mesozoic, undivided. Others: 9 – foliation cleavage, 10 – faults, 11 – overthrusts, 12 – overthrust line of nappes.
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ranging from 0.4 to 2.2 % (Table 2). Quartz grains are the
dominant detrital component, with monocrystalline (Qm)
prevailing over polycrystalline (Qp) quartz. An exception is
the sample 22-VD, where the Qp is dominant. The values of
the Qm/Qp ratio vary in the range of 0.7—5.0. The fragments
of potassium and Na-Ca feldspars are in equal abundances,
but with potassium feldspars slightly prevailing over pla-
gioclases. For this reason, the ratio of potassium feldspars
(K) to plagioclases (P) shows mostly the values near 1 (K/
P = 0.8—1.7).
However, in the sample 33-VD this ratio is higher than 5,
as the potassium feldspar highly prevails (Table 2). The po-
tassium feldspars in the studied samples are represented by
orthoclase (Ab
10.2—3.4
An
0.3—0.1
Or
89.5—96.5
) and by microcline.
The Na-Ca feldspars correspond to albite—oligoclase (An
0.3—
25.4
). Generally, they manifest a low content of orthoclase
component (Or
0.1—1.5
). Alterations of detrital feldspars during
post-sedimentary processes were studied by V ačný (2013),
who found that the secondary albitization of feldspars did
not reflect diagenetic changes, but modification processes in
the primary source area.
Clastic mica content varied in the range of 0—8 % (Ta-
ble 2). Lithic fragments varies similarly. Volcanic rock frag-
ments (0 to 19 %) are represented by acid, as well as
andesite-basalt rocks. Likewise, the content of metamorphic
rock fragments is irregular (0—18 %), among them, the dif-
ferent phyllites and metaquartzites are most widespread.
Fragments of the fine-grained paragneisses and mica schists
are present only in minor amounts. According to the mineral
composition, the studied sandstones belong to the arkoses,
subarkoses, lithic subarkoses, and feldspathic litharenites
(classification after McBride 1963).
The assemblage of heavy minerals includes: biotite
(29.5 ± 32 %), magnetite, ilmenite and hematite (27 ± 26 %),
titanite (14 ± 12 %), tourmaline (10 ± 10 %), garnet (9 ± 8 %),
apatite (6 ± 7 %), zircon (4 ± 3 %), and rutile (0.5 ± 0.9 %).
These data represent the average from the ten analysed sand-
stone samples (V ačný 2013).
Analytical technique
Monazite grains were only sporadically recorded in the
heavy-mineral fraction using the gravity separation method in
heavy liquids. The dried samples were sieved (0.063—
0.250 mm) for the heavy mineral analyses. As the monazite
formed the small grains (predominant 10—50 µm, seldom
around 100 µm) and the relatively scarce larger grains were of-
ten destroyed during disintegration of the sandstones, monazites
were not detected within the heavy mineral assemblage. Conse-
quently, all analyses of monazites were carried out on the grains
found in the polished thin sections by microprobe analysis.
Analyses of monazites were obtained using the electron mi-
croprobe Cameca SX-100 housed at the Department of Spe-
cial Laboratories at the State Geological Institute of Dionýz
Štúr (Geological Survey of Slovak Republic) in Bratislava.
Monazite analyses suitable for dating have to meet some spe-
cial analytical conditions. The counting time for Pb was ex-
tended to 300 s and the beam current adjusted to 180 nA.
Accelerating voltage of 15 kV can efficiently excite the
PbMa line. The beam diameter of 3 µm was used. These con-
ditions form a compromise between two cases: maximizing
counts while minimizing damage effect at the beam spot.
The other elements involved in the dating calculations also
had prolonged counting times, Th 35 s, U 90 s, Y 45 s. The
following calibration standards (natural grains or synthetic
compounds) and analytical lines were used: apatite (PK
α),
wollastonite (SiK
α, CaKα), GaAs (AsLα), barite (SKα,
BaL
α), Al
2
O
3
(AlK
α), ThO
2
(ThM
α), UO
2
(UM
β), cerusite
(PbM
α), YPO
4
(YL
α), LaPO
4
(LaL
α), CePO
4
(CeL
α), PrPO
4
(PrL
β), NdPO
4
(NdL
α), SmPO
4
(SmL
α), EuPO
4
(EuL
β),
GdPO
4
(GdL
α), TbPO
4
(TbL
α), DyPO
4
(DyL
β), HoPO
4
(HoL
β), ErPO
4
(ErL
β), TmPO
4
(TmL
α), YbPO
4
(YbL
α),
LuPO
4
(LuL
β), fayalite (FeKα) and SrTiO
3
(SrL
α). Mutual
interferences U-M
β with ThMα, ThM3-N4, ThM5-P3 and
PbM
α with ThMζ
1
, ThM
ζ
2
, YL
γ
2,3
and various interferences
between REE’s were resolved by using correction coeffi-
cients derived by measurement on the calibration standards.
A complete analysis of monazite involving almost all ele-
ments present in monazite is obtained at each measurement
spot. The age calculated from one point is referred to as the
Table 2: Modal compositions of the studied Permian sandstones
from the Malužiná Formation.
Sample Sample locality
GPS coordinates
19-VD
Loc. MK-12; southern slope of the Klokoč hill; 425 m above sea level
N 48º28'401”, E 17º19'181”
22-VD
Loc. MK-15; Sološnická dolina valley, right side of the Sklenný vrch hill; 457 m above sea level
N 48º27'008”, E 17º17'556”
23-VD
Detto loc. MK-15
N 48º27'008”, E 17º17'556”
31-VD
Loc. MK-20; left tributary of the Sološnická dolina valley, east of the Peterklin hill; 280 m above sea level N 48º26'643”, E 17º14'904”
32-VD
Loc. MK-21; southwestern ridge of the Klokoč hill, west of the Mesačná hill; 470 m above sea level
N 48º27'602”, E 17º17'838”
33-VD
Loc. MK-22; south-west valley from the Klokoč hill; 444 m above sea level
N 48º27'422”, E 17º17'942”
Table 1: List of the studied sandstone samples and their locations.
Sample
Qm
(%)
Qp
(%)
P
(%)
K
(%)
Lm
(%)
Lv
(%)
Mt
(%)
Mc
(%)
19-VD
56.0
17.0
10.1
13.9
0.0
0.0
2.0
1.0
22-VD
20.1 26.8 10.1 11.0 18.3 10.3 0.9 2.5
23-VD
26.1 21.0 10.8 12.1 13.0
8.3 0.4 8.3
31-VD
26.9 17.1 15.5 12.7
5.0 19.0 1.8 2.0
32-VD
37.9
26.7
10.4
17.4
1.7
3.9
1.4
0.6
33-VD
60.4
12.2
3.2
19.3
2.4
0.2
2.2
0.0
Explanations: Qm – monocrystalline quartz grains, Qp – polycry-
stalline quartz grains, P – plagioclase feldspar grains, K – potassium
feldspar grains, Lm – metamorphic lithic grains, Lv – volcanic-hy-
pabyssal lithic grains, Mt – matrix, Mc – mica.
Abbreviations of
petrofacies parameters (Qp, Qm, K, P) were used after Dickinson &
Suczek (1979) and Dickinson (1985, 1988).
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Fig. 2. BSE images showing the Permian (A, B) and the Variscan (C—H) monazites in various samples.
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apparent age. Groups of the apparent ages plotted in a histo-
gram indicate a single age population. An isochrone diagram
provides a further test to distinguish single age populations.
Points should plot on a single line crossing the zero coordi-
nate. The method of age calculation based on the statistical
approach was described by Montel et al. (1996). The preci-
sion of monazite dating was proven by dating of seven mon-
azite standards dated by SHRIMP. The error in age was
determined by error propagation from 2
σ errors obtained for
measured Pb, Th and U though equation of age. For these el-
ements the 2
σ error was added or subtracted, giving six con-
centrations that were used for the age determination in all
possible mutual combinations. Finally, the age error was taken
according to biggest deviation from the age obtained from
measured Pb, Th and U concentrations.
Histograms and isochrones were constructed using the au-
thor’s own unpublished software (Mondat in Excel spread-
sheet, P. Konečný). Monazite age was calculated following
the statistical procedure after Montel et al. (1996).
Monazite features and chemical composition
Dating of monazites from the MF sandstones revealed two
distinct age populations, Permian and Carboniferous. The
monazite populations differ in shape, zoning and chemical
composition. The Carboniferous monazites are usually bigger,
having the diameter from 20 to 120 µm and often showing a
complex chemical zoning (BSE images, Fig. 2H). On the other
hand, monazites of Permian age are smaller, with a size of
about 10 to 30 µm, and have homogeneous composition. Only
few grains show zoning in BSE images. Although the mona-
zites of the both age populations are chemically similar, they
have some specific features. The range of Th* presented in the
isochrone diagrams (Figs. 4, 5) is very wide for the Carbonif-
erous monazites from 3.98 to 11.27 Th*, whereas the Permian
monazites have lower Th* limited to a range from 2.85 to 6.07
and one grain with 8.58. ThO
2
content is similar in both mona-
zite groups. For the Carboniferous monazites the average ThO
2
is 4.8 wt. % (min 2.1, max 10.2) and for Permian average con-
tent is 4.6 wt. % (min 2.5, max 6.5). The Carboniferous mona-
zites are roughly three times more enriched in UO
2
, with the
average for the Carboniferous monazites 0.66 wt. % (min 0.16,
max 2.43) and for the Permian monazites 0.26 wt. %.
The Carboniferous monazites contain slightly less REE’s
than the Permian ones. Enrichment in REE for the Permian
monazites is due to higher content of La and Ce. Average con-
tent of La
2
O
3
for the Carboniferous monazites is 13.23 wt. %
(min 11.04, max 15.99) and for the Permian 14.49 wt. %
(min 11.04, max 17.80). Ce behaves similarly, the Carboniferous
monazites have an average Ce
2
O
3
of 28.24 wt. % (min 25.79,
max 30.17), the average for the Permian grains is 29.59 wt. %
Ce
2
O
3
(min 26.46, max 32.69). Abundance of Pr, Nd and Sm
is almost identical for the both age groups. Yttrium is higher in
the Carboniferous monazites with average of 1.61 wt. % Y
2
O
3
(min 0.42, max 2.96) and 1.36 wt. % (min 0.18, max 3.87) for
the Permian monazites. The monazites of Carboniferous and
Permian age contain negligible concentrations of S and Sr.
Some of the monazites have As up to 0.1 wt. %.
Monazite compositional variations are affected by the sub-
stitution processes. The most common substitutions are hut-
tonite and cheralite substitutions (after Linthout 2007). The
composition of the Carboniferous and the Permian mona-
zites involves both types of substitutions (Fig. 3). The Car-
boniferous monazites tend to follow the huttonite exchange
vector, while the Permian monazites are shifted towards the
cheralite substitution.
Monazite dating
Monazite dating presented on a histogram proves two
main events: Carboniferous and Permian.
A substantial part of the analysed monazites (54 out of
72 data, that is about 70 % of all measurements) showed
the peak of Variscan age, in the histogram with dominance
of apparent ages in the range of 340—371 Ma (Fig. 4, Ta-
ble 3 – only as a Suplemment in the electronical version;
www.geologicacarpathica.com), which corresponds to the
interval from Famennian to Lower Visean according to the
International Stratigraphic Chart (2008). Some outliers occur
on both sides of the age histogram. Two monazite ages were
somewhat older, 391 Ma (sample 33-VD) and 401 Ma (sam-
ple 31-VD) which correspond to the boundary of the Lower/
Middle Devonian (Emsian—Givetian).
Likewise, no more than four grains showed younger ages,
spanning the range from 311 to 323 Ma, that corresponds to
the Serpukhovian—Bashkirian according to the International
Stratigraphic Chart (2008). The Variscan age calculated for
monazites within the interval 330—380 Ma from 48 grains
(Fig. 4) is 351 ± 3.3 Ma, corresponds to the earliest Tournai-
sian, or the stratigraphic boundary between the Devonian
and the Carboniferous (Famennian—Tournaisian). The wide
range of Th* enables us to construct an isochron which
crosses the origin at a very small deviation + 3 3 ppm Pb
(equation of the linear trend is y = 0.0151x + 0.0033).
Fig. 3. Substitutions in monazites from the Malužiná Formation
sandstones. Different symbols refer to the Mississippian (cross) and
Permian monazites (circle).
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Besides the Devonian-Carboniferous ages, Permian ages
(Table 3) were also detected in the two samples (19-VD and
22-VD). Histogram (Fig. 5) presents the significant maxi-
mum around 255 Ma. The weighted average corresponds to
255 ± 6.2 Ma. All data represent a perfect, almost ideal isoch-
ron with parameters y = 0.0113x + 0.0003 which crosses the
origin at + 3 ppm Pb.
Only a few measurements gave the Triassic ages in the in-
terval 240—230 Ma. Because the samples containing monazite
with Triassic ages are situated either directly along the thrust
nappe plane of the Hronicum Unit (22-VD) or within the zone
of Cu ± U-bearing mineralization (19-VD), we suppose that
these ages reflect the local alterations of the Permian detrital
monazite by the circulations of the low-temperature hydro-
thermal fluids.
Discussion
Variscan provenance
: Age data as inferred from the chem-
ical monazite dating of the Permian clastic sediments of the
Hronicum Unit are practically missing. Only Olšavský (2008)
in his Ph.D. Thesis (results previously presented at the 6
th
Anni-
versary seminary of the Slovak Geological Society – Demko
& Olšavský 2007) provided about 40 monazite ages from the
southern slopes of the Nízke Tatry Mts, but only in the form
of a enclosed histogram and without an accompanying table of
complete data on chemical composition. Also with respect to
interpretation, it is important to state here that these monazite
ages came from rhyolite fragments separated from gravel ma-
terial in the MF coarse-grained conglomerates, from the hang-
ing wall of andesite/basalts of the second eruption phase at the
locality of Bystrá-Stupka. Olšavský’s (2008) data show the bi-
modal dispersal of monazite ages. The first group hints at the
Permian ages, with a striking peak at 290 Ma, in the range of
230—290 Ma, with the weighted average of 257 ± 9 Ma (20 anal-
yses). The second age group displays the peak at 360 and
340 Ma, whereby age dispersal is relatively wide (from 310 to
370 Ma), with the weighted average of 342 ± 12 Ma (22 analy-
ses), corresponding to the Visean. Detected age maxima sug-
gest two phases of volcanic activity: one phase took place in
the Cisuralian and the second one in the Mississippian.
Basically, very similar age data were also detected from
detrital monazites of the MF sandstones in the Malé Karpaty
Fig. 5. A – Frequency diagrams of the Permian/Triassic monazite ages in the Malužiná Formation sandstone samples (data source see Ta-
ble 3). B – Pb vs Th* plot of single analyses and drawn isochrones from 100 to 500 Ma. Th* is given by measured Th plus added U recal-
culated to Th equivalent concentration, after natural decay leading to Pb production.
Fig. 4. A – Histogram showing the whole distribution of the Variscan EMPA monazite ages obtained from the Malužiná Formation sand-
stones, with indication of the peak ages (data source see Table 3). B – Pb vs Th* plot of single analyses and drawn isochrones from 100 to
500 Ma. Th* is given by measured Th plus added U recalculated to Th equivalent concentration, after natural decay leading to Pb production.
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Mts. The weighted average monazite age of 351 ± 3.3 Ma
(Fig. 4), detected in the sandstone samples of the MF in the
Malé Karpaty Mts, is similar to the monazite ages inferred
from the rhyolite pebbles of the MF on the southern slopes
of the Nízke Tatry Mts. It is unquestionable that the detected
Mississippian monazite ages indicate the age of the source
area of the MF sediments. It is evident that acid volcanic
rocks are one of the sources, as described in the case of oc-
currences of the MF on the southern slopes of the Nízke Tatry
Mts by Olšavský (2008). In the studied MF sandstones from
the Malé Karpaty Mts, content of acid volcanic fragments
vary in the range from 0 to 19 volumetric % (Table 2). How-
ever, it is important to stress that fragments of rhyolites rep-
resent a common component of the clastic detritus in the
whole profile of the MF Permian sediments of the Hronic
Unit, not only in the form of pebbles in conglomerates but
also in the form of lithic grains in sandstones (Ďurovič 1971;
Vozárová & Vozár 1988; Vozárová 1990, 1998; Olšavský
2008; V ačný 2013; V ačný et al. 2013).
In the pre-Pennsylvanian crystalline basement of the central
Western Carpathians, several low-grade metamorphosed com-
plexes occur (confr. Biely et al. 1996), that mostly emerge in
the form of tectonically restricted slices on the middle- and
higher metamorphosed complexes, or they lie directly on
granitoids. Some of them even show features of contact meta-
morphosis. In fact, products of acid volcanism were found
only in the Jánov Grúň Complex (Bajaník et al. 1979; Miko
1981) in the Krá ovoho ské Tatry Mts and in the Krak ová
Formation (Korikovskij & Miko 1992), both emerging in the
Northern Veporic Unit. The volcanics together with their effu-
sive members make up conformal layers with metasediments,
alternating with each other, as is usual with synsedimentary
volcanism. On the basis of pollen analysis of associated
metasediments, the Jánov Grúň Complex was broadly strati-
graphically classified into the Upper Silurian to the Mississip-
pian (Klinec et al. 1975; Planderová & Miko 1977). Likewise,
on the basis of the U-Pb (SHRIMP) zircon ages, the Mississip-
pian age of 358.7 ± 3.9 Ma was detected from the metarhyo-
lites of the low-grade crystalline basement of the Krak ová
Zone from the Volchovo valley (Vozárová et al. 2010). Bio-
stratigraphically well documented Mississippian metasedi-
ments are known only from the Northern Gemeric Unit
(Bouček & Přibyl 1960; Kozur et al. 1976; Bajaník & Plande-
rová 1985; Mamet & Mišík 2003). They were originally de-
scribed as the Ochtiná Formation (Bajaník et al. 1981) and
later were redefined as the separate Ochtiná Group (Vozárová
1996). However, the problem remains that no synsedimentary
acid volcanics are known within the Ochtiná Group sequence.
Monazite ages from the rhyolite fragments detected on the
southern slopes of the Nízke Tatry Mts (Demko & Olšavský
2007; Olšavský 2008) and also from sandstones of the MF in
the Malé Karpaty Mts given in the present work, are in
agreement with the upper boundary of the stratigraphic clas-
sification of microflora from the Jánov Grúň Complex. We
assume that low-grade crystalline complexes must have existed
in the source area of the MF sediments. They were similar to
the occurrences in the Krak ová and ubietová Zones of the
crystalline basement of the Northern Veporic Unit that in-
cluded horizons with acid volcanism of the Mississippian age.
However, the acid volcanites were not the exclusive
source of detrital monazite. In comparison with rhyo-dacitic
detritus, detrital material derived from granitoid complexes
(potassium feldspars, Na-Ca feldspars, clastic mica), is the
substantially more conspicuous clastic component in the
sandstones of the MF (Table 2). Likewise, granitoid pebbles
are common in associated conglomerates. No doubt a sub-
stantial part of the detrital monazites were derived from the
plutonic complexes.
In the Western Carpathians, magmatic plutons intruded
into the high- to medium-grade crystalline basement made of
upper- and middle-crustal Variscan nappes (Bezák et al.
1997) which show distinct southern vergency (Siegl 1982;
Putiš 1992; Bezák et al. 1997; Bielik et al. 2004). The prevail-
ing granitoids are petrochemically classified as the S-types.
Granodiorite-tonalite I-types are relatively less represented.
Permian A-type granitoides and volcanics are spatially least
wide-spread (Broska & Uher 2001; Poller et al. 2002; Kohút
& Stein 2005; Radvanec et al. 2009; Uher et al. 2009;
Vozárová et al. 2009, 2012). U-Pb zircon radiometric dat-
ings confirmed the range from Devonian to Permian for the
Variscan magmatic period in the Western Carpathians
(Bibikova et al. 1988; Kohút et al. 1997, 2009; Krá et al.
1997; Poller & Todt 2000; Gaab et al. 2006; Broska et al.
2013 and references therein). According to the original age
data, it was assumed that S-type granitoids are systematically
older, with the range of 340—367 Ma, while I-types of grani-
toids are younger, with the range of 303—345 Ma. Likewise,
monazite ages also showed similar age discrepancies, with
the range of 333—367 Ma for S-types and of 308—345 Ma for
I-types (Finger et al. 2003 and references therein). However,
this assumption of different ages for S- and I-types of grani-
toids was rebutted by new SIMS U-Pb zircon ages that con-
firmed the Mississippian age, within the range of
367—353 Ma also for I-type granitoids. Therefore, almost the
same age was documented for both I- and S-type magmatites
(Broska et al. 2013).
The ages of detrital monazites detected in the MF sand-
stones from the Malé Karpaty Mts dominantly span the
range from 340 to 370 Ma. This is the period that covers the
maximal intensity of the Variscan polyphase magmatic ac-
tivity in the Western Carpathians. Petrofacies analyses of the
Permian sandstones from the Hronicum Unit in all occur-
rences in the Western Carpathians suggest provenances either
from dissected magmatic arc or active continental margin
(Vozárová & Vozár 1988; Vozárová 1990; V ačný et al.
2013). Mixing of magmatogenic and volcanogenic detritus,
associated only with a small amount of low- to medium-
grade metamorphic clasts is characteristic (Dickinson &
Suczek 1979; Dickinson 1985, 1988; Ingersoll 1990). The
chemical composition of clastic detritus in the MF sand-
stones from the Malé Karpaty Mts also indicates the acid to
intermediate magmatic provenance, similar to active conti-
nental margin (V ačný et al. 2013). On the basis of petro-
chemical data and age of detrital monazites, we can infer the
source area of the MF sandstones to be most likely derived
from I-type magmatism associated with the Variscan sub-
duction processes and with the origin of magmatic arc in the
Mississippian. Stampfli (2012) regards I-types granitoids as
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an indicator of the onset of the subduction process of the
Prototethys. Alternatively, Broska et al. (2013) also infer for-
mation of I-type granitoids in the Western Carpathians from
the Variscan magmatic arc, as a result of collision of the Pro-
totatricum crust (the term Prototatricum was used by these
authors for the common Variscan basement of the Tatric and
the Veporic Units) which was a part of the Galatian superter-
rane, with the oceanic crust of the Prototethys.
The metarhyodacite fragments occur, as a whole, in the
Pennsylvanian-Permian clastic sediments of the Hronicum
Unit in the Western Carpathians and it is considered that
acid volcanism was synchronous with the main magmatic
events in the Mississippian. These volcanic centers were
probably situated in the former back-arc basins on the conti-
nental crust or directly in the intra-arc environment. In the
Veporicum Unit the low-grade acid volcanite-bearing crys-
talline complexes were tectonically overthrusted onto the
higher-grade crystalline complexes. This was a result of not
only Alpine but also probably already Variscan tectonics as
a part of them were overlapped by the Permian sediments.
Permian provenance
: The Permian monazite ages show
the significant maximum at 255 Ma, with the weighted aver-
age of 255 ± 6.2 Ma. Monazites were most likely derived
from synsedimentary volcanic sources that could be situated
on the margins of the original Pennsylvanian-Permian sedi-
mentary rift of the Hronicum Unit. These monazite age data
are similar to the 260 Ma of
87
Rb/
86
Sr age of the basalt sam-
ple from the 2
nd
eruption phase (Vozárová et al. 2007) and
roughly correspond to radiometric U-Pb dating of the urani-
um mineralization (Legierski in Rojkovič 1997 – Kravany
Beds, 263—274 Ma) from the Nízke Tatry Mts.
The original sedimentary basin of the Ipoltica Group, based
on the characteristic sedimentary filling, as well as the distri-
bution of sedimentary lithofacies and narrow connection with
linear continental tholeiitic volcanism, permits to incorporate
this sedimentary basin into the regional rift system of several
kilometers long. Marginal parts and basement of the original
sedimentary basin were tectonically cut off due to the Alpine
nappe stacking. In the recent structure of the Western Car-
pathians, the rootless nappes of the Hronicum Unit (Biely &
Fusán 1967; Biely et al. 1968; Andrusov et al. 1973) have
preserved only the central parts of the original sedimentary
basin, with its occurrences of andesite-basalt continental
tholeiites. The acid volcanites, belonging to the supposed
primary bimodal volcanic association, are only present as the
redeposited rhyo-dacite detritus in clastic sediments (peb-
bles, sand grains).
A small number of monazite grains show analytical spots
with younger ages (Fig. 2A), within the interval of 230—
240 Ma. This rejuvenation reflects an alteration of the original
Permian monazites by the circulated low-thermal fluids during
diagenetic processes. These younger monazite ages were
mainly detected on the grains from the area of synsedimentary
Cu ± U mineralization (west and southwest from Sološnica;
Rojkovič 1997 and references therein). Because the Hronicum
Permian sedimentary basin was situated in arid climatic condi-
tions as a whole, the circulated diagenetic fluids were charac-
terized by high salinity. Thus, the highly saline brines could
have started the rejuvenation of the Permian detrital monazite
by migration of some elements. A detailed explanation of this
process was described by Mathieu et al. (2001) in U deposits
of the Franceville basin, Gabon.
Conclusions
The chemical ages of detrital monazites from the MF Per-
mian sandstones of the Hronic Unit in the Malé Karpaty Mts
show two maxima: i) Variscan ages with maximal peaks in
the range of 370—340 Ma, with a weighted average of
351 ± 3.3 Ma and, ii) Permian ages in the interval of 280—
250 Ma, with the distinct peak at 255 Ma. These two age
groups reflect several different sources of clastic detritus for
the Permian sediments of the Hronicum Unit. Variscan mag-
matic rocks, bounded with subduction-collisional magmatic
arc, appear to be the main source. They correspond to zircon
and also monazite ages described from I-type magmatites of
the Western Carpathians. Presumably, the partial mixture
with an S-type magmatic source cannot be excluded. The
same Variscan monazite age was derived from the acid
metavolcanic rocks connected with the low-grade metamor-
phic crystalline complexes. The additional sources were the
Permian rhyo-dacite synsedimentary volcanic centers, situated
on the rifted, fault-bordered margins of the original sedimen-
tary basin.
The Permian rift-related sedimentary basin of the Hroni-
cum Unit was situated in a foreland retro-arc setting on the
Prototatricum (in the sense of Broska et al. 2013) continental
crust. This sedimentary basin was filled with clastic detritus
derived from a dissected Mississippian magmatic arc and
Permian synsedimentary volcanic centers.
Acknowledgments: We would like to express our gratitude
to the reviewers F. Finger, R. Čopjaková and I. Broska for
their helpful and critical comments on the earlier versions of
the manuscript. This work was supported by the Slovak Re-
search and Development Agency under the Contract No.
APVV-0546-11 and the Slovak Scientific Grant Agency
(Grant No. VEGA-1/0095/12).
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Article
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VOZÁROVÁ et al.: Provenance of Permian Malužiná Formation sandstones (Hronicum, Western Carpathians): evidence from monazite geochronology
Appendix 1
Table 3: Microprobe analyses of monazites from the Malužiná Formation sandstones used for monazite dating. All analyses calculated on the 16 oxygen. Abbreviations: bdl. – denotes below
detection limit. C. – Carboniferous; P. – Permian.
Sample
19-VD
Point 1/1 2/1 2/2 3/1 3/2 4/1 4/2 5/1 6/1 7/1 8/1 9/1 10/1
11/1 8/1 9/1 10/1 4/3 7/2 8/2 9/2 10/2
10/3
11/2
11/3
11/4
C. C. C. C. C. P. P. C. C. P. P. C. P. P. P. C. P. P. P. P. C.. P. P. P. P. P.
P
2
O
5
30.02 29.21 29.12 29.02 29.21 28.61 28.61 28.20 28.35 30.22 30.19 29.50 29.43 29.90 30.19 29.50 29.43 29.02 29.81 29.64 29.30 29.41 29.36 29.29 29.45 28.93
As
2
O
5
0.13 0.15 0.14 0.13 0.15 0.14 0.15 0.13 0.14 0.13 0.14 0.14 0.14 0.14 0.14 0.14 0.14 0.15 0.13 0.15 0.15 0.14 0.15 0.15 0.14 0.15
SiO
2
0.47 0.45 0.46 0.57 0.49 0.76 0.67 1.14 0.87 0.39 0.20 0.59 0.55 0.40 0.20 0.59 0.55 0.75 0.22 0.21 0.73 0.51 0.62 0.72 0.60 0.93
ThO
2
6.15 5.44 6.11 5.87 5.82 4.54 3.94 8.68 6.15 5.87 2.75 5.00 5.73 5.60 2.75 5.00 5.73 4.58 4.29 3.09 5.61 5.01 5.78 5.31 5.43 5.27
PbO
0.14 0.08 0.10 0.10 0.11 0.05 0.05 0.14 0.10 0.07 0.03 0.08 0.07 0.10 0.03 0.08 0.07 0.05 0.06 0.04 0.09 0.06 0.07 0.07 0.07 0.06
UO
2
0.96 0.17 0.25 0.43 0.40 0.12 0.09 0.47 0.20 0.37 0.18 0.18 0.18 1.30 0.18 0.18 0.18 0.10 0.56 0.16 0.17 0.16 0.18 0.34 0.30 0.18
Y
2
O
3
1.16 0.57 1.44 2.01 1.96 0.49 0.48 2.23 0.98 3.40 1.15 0.96 1.42 3.00 1.15 0.96 1.42 0.52 3.87 0.91 0.72 1.27 1.42 1.62 2.48 1.02
La
2
O
3
14.91 14.33 11.86 11.04 11.39 17.21 17.80 12.08 14.54 11.35 14.69 15.77 13.60 11.04 14.69 15.77 13.60 17.35 11.13 14.45 15.99 14.15 13.62 13.59 13.02 15.20
Ce
2
O
3
28.15 29.61 27.47 27.48 27.76 30.68 30.87 26.26 29.12 26.46 30.46 30.10 28.87 26.53 30.46 30.10 28.87 30.70 26.61 30.10 30.02 29.37 28.90 29.04 27.95 29.96
Pr
2
O
3
3.11 3.44 3.37 3.40 3.48 3.17 3.24 3.15 3.29 3.30 3.56 3.30 3.34 3.29 3.56 3.30 3.34 3.23 3.33 3.44 3.20 3.35 3.32 3.32 3.34 3.29
Nd
2
O
3
11.34 12.73 12.52 12.96 13.16 11.73 11.43 11.57 11.67 12.56 13.24 11.80 12.50 12.35 13.24 11.80 12.50 11.83 12.61 13.43 11.55 12.64 12.49 12.74 12.53 11.92
Sm
2
O
3
2.17 2.08 2.92 2.83 2.75 1.57 1.57 2.64 2.03 2.96 2.32 1.91 2.46 3.16 2.32 1.91 2.46 1.60 3.10 2.30 1.80 2.26 2.28 2.44 2.45 1.90
Eu
2
O
3
0.08 0.02 0.01 0.11 0.17 0.03 0.03 0.12 0.10 bdl. 0.05 0.03 0.03 bdl. 0.05 0.03 0.03 bdl. 0.01 0.03 0.03 bdl. 0.01 0.00 0.03 0.01
Gd
2
O
3
1.20 0.83 1.67 1.60 1.17 0.57 0.52 1.41 0.91 1.91 1.08 0.94 1.31 1.90 1.08 0.94 1.31 0.37 1.82 0.87 0.52 0.92 1.01 0.97 1.25 0.60
Tb
2
O
3
0.06 0.08 0.16 0.16 0.13 0.04 0.08 0.18 0.10 0.22 0.05 0.02 0.06 0.24 0.05 0.02 0.06 0.07 0.21 0.09 0.09 0.06 0.09 0.14 0.16 0.06
Dy
2
O
3
0.47 0.19 0.49 0.64 0.61 0.20 0.18 0.65 0.31 0.97 0.31 0.30 0.41 0.94 0.31 0.30 0.41 0.10 1.12 0.37 0.24 0.40 0.45 0.53 0.69 0.40
Ho
2
O
3
0.06 0.02 0.03 0.05 0.02 bdl. bdl. 0.08 0.03 0.08 0.01 0.01 0.04 0.09 0.01 0.01 0.04 bdl. 0.13 0.01 0.02 0.03 0.05 0.06 0.10 0.06
Er
2
O
3
0.36 0.33 0.40 0.45 0.41 0.33 0.30 0.38 0.32 0.48 0.35 0.36 0.35 0.48 0.35 0.36 0.35 0.26 0.54 0.35 0.32 0.40 0.35 0.41 0.47 0.40
Tm
2
O
3
0.05
0.04
0.06
0.06
0.06
0.07
0.03
0.05
0.06
0.08
0.04
0.07
0.05
0.05
0.04
0.07
0.05
0.03
0.08
0.05
0.06
0.05
0.07
0.07
0.09
0.05
Yb
2
O
3
0.14 0.12 0.12 0.16 0.11 0.09 0.09 0.15 0.09 0.19 0.10 0.14 0.16 0.19 0.10 0.14 0.16 0.10 0.18 0.13 0.12 0.11 0.12 0.12 0.13 0.14
Lu
2
O
3
0.07 0.12 0.13 0.06 0.12 0.10 0.09 0.06 0.10 0.05 0.14 0.07 0.01 0.09 0.14 0.07 0.01 0.06 0.09 0.09 0.08 0.10 0.08 0.16 0.09 0.05
FeO
bdl. bdl. 0.01 bdl. bdl. bdl. bdl. bdl. bdl. 0.01 0.02 bdl. 0.00 0.05 0.02 bdl. 0.00 bdl. bdl. 0.02 bdl. bdl. 0.00 0.08 0.05 0.22
SO
3
0.03 0.02 0.03 0.43 0.37 0.02 0.04 0.09 0.35 0.02 0.02 0.04 0.03 0.01 0.02 0.04 0.03 0.03 0.03 0.02 0.03 0.02 0.04 0.02 0.02 0.02
CaO
1.36 1.07 1.17 1.45 1.40 0.47 0.47 1.14 1.11 1.17 0.61 0.69 0.89 1.26 0.61 0.69 0.89 0.50 1.03 0.67 0.70 0.76 0.88 0.69 0.81 0.48
SrO
0.00 0.02 0.01 0.03 0.03 bdl. 0.02 0.02 bdl. 0.04 0.00 0.02 0.01 bdl. 0.00 0.02 0.01 0.00 0.01 0.03 0.02 0.01 bdl. 0.01 0.01 0.00
Al
2
O
3
bdl. bdl. 0.00 bdl. bdl. bdl. bdl. bdl. bdl. bdl. bdl. bdl. bdl. bdl. bdl. bdl. bdl. bdl. bdl. bdl. bdl. bdl. bdl. bdl. bdl. bdl.
Total
102.60 101.13 100.06 101.06 101.27 100.99 100.77 100.99 100.90 102.31 101.71 102.02 101.64 102.10 101.71 102.02 101.64 101.41 100.96 100.65 101.59 101.19 101.34 101.91 101.65 101.30
P
3.904 3.880 3.892 3.822 3.839 3.828 3.834 3.766 3.775 3.912 3.947 3.876 3.878 3.898 3.947 3.876 3.878 3.848 3.914 3.931 3.866 3.889 3.875 3.854 3.869 3.834
Si
0.071 0.070 0.072 0.088 0.076 0.121 0.107 0.179 0.136 0.059 0.031 0.091 0.085 0.061 0.031 0.091 0.085 0.118 0.035 0.033 0.114 0.079 0.097 0.112 0.093 0.145
As
0.010 0.013 0.012 0.011 0.012 0.012 0.012 0.011 0.012 0.011 0.011 0.012 0.011 0.011 0.011 0.012 0.011 0.012 0.011 0.012 0.012 0.011 0.012 0.012 0.011 0.012
Th
0.215 0.194 0.220 0.208 0.206 0.163 0.142 0.312 0.220 0.204 0.097 0.177 0.203 0.196 0.097 0.177 0.203 0.163 0.151 0.110 0.199 0.178 0.205 0.188 0.192 0.188
U
0.033 0.006 0.009 0.015 0.014 0.004 0.003 0.016 0.007 0.013 0.006 0.006 0.006 0.045 0.006 0.006 0.006 0.004 0.019 0.006 0.006 0.005 0.006 0.012 0.010 0.006
Pb
0.006 0.004 0.004 0.004 0.004 0.002 0.002 0.006 0.004 0.003 0.001 0.003 0.003 0.004 0.001 0.003 0.003 0.002 0.002 0.002 0.004 0.003 0.003 0.003 0.003 0.003
Y
0.095 0.047 0.121 0.167 0.162 0.041 0.041 0.187 0.082 0.277 0.095 0.079 0.118 0.246 0.095 0.079 0.118 0.044 0.320 0.076 0.060 0.106 0.117 0.134 0.205 0.085
La
0.845 0.829 0.691 0.634 0.652 1.004 1.039 0.703 0.843 0.640 0.837 0.903 0.781 0.627 0.837 0.903 0.781 1.002 0.637 0.835 0.919 0.815 0.783 0.779 0.745 0.878
Ce
1.583 1.701 1.588 1.565 1.578 1.776 1.789 1.517 1.677 1.481 1.722 1.710 1.645 1.496 1.722 1.710 1.645 1.761 1.511 1.726 1.713 1.679 1.649 1.653 1.588 1.717
Pr
0.174 0.197 0.194 0.193 0.197 0.182 0.187 0.181 0.189 0.184 0.200 0.186 0.190 0.185 0.200 0.186 0.190 0.184 0.188 0.196 0.182 0.191 0.188 0.188 0.189 0.188
Nd
0.622 0.714 0.706 0.720 0.729 0.662 0.646 0.652 0.656 0.686 0.730 0.654 0.695 0.679 0.730 0.654 0.695 0.662 0.698 0.751 0.643 0.705 0.696 0.708 0.694 0.666
Sm
0.115 0.113 0.159 0.152 0.147 0.086 0.086 0.144 0.110 0.156 0.124 0.102 0.132 0.168 0.124 0.102 0.132 0.087 0.166 0.124 0.097 0.122 0.123 0.131 0.131 0.103
Eu
0.004 0.001 0.000 0.006 0.009 0.002 0.002 0.006 0.005 0.000 0.002 0.002 0.001 0.000 0.002 0.002 0.001 0.000 0.000 0.002 0.002 0.000 0.001 0.000 0.002 0.001
Gd
0.061
0.043
0.087
0.082
0.060
0.030
0.027
0.074
0.047
0.097
0.055
0.048
0.068
0.097
0.055
0.048
0.068
0.019
0.093
0.045
0.027
0.047
0.052
0.050
0.064
0.031
Tb
0.003 0.004 0.008 0.008 0.007 0.002 0.004 0.009 0.005 0.011 0.002 0.001 0.003 0.012 0.002 0.001 0.003 0.004 0.011 0.005 0.005 0.003 0.004 0.007 0.008 0.003
Dy
0.023 0.010 0.025 0.032 0.030 0.010 0.009 0.033 0.016 0.048 0.015 0.015 0.021 0.047 0.015 0.015 0.021 0.005 0.056 0.019 0.012 0.020 0.023 0.027 0.035 0.020
Ho
0.003 0.001 0.002 0.003 0.001 0.000 0.000 0.004 0.002 0.004 0.000 0.000 0.002 0.004 0.000 0.000 0.002 0.000 0.006 0.000 0.001 0.002 0.002 0.003 0.005 0.003
Er
0.017 0.016 0.020 0.022 0.020 0.016 0.015 0.019 0.016 0.023 0.017 0.018 0.017 0.023 0.017 0.018 0.017 0.013 0.026 0.017 0.016 0.020 0.017 0.020 0.023 0.019
Tm
0.002 0.002 0.003 0.003 0.003 0.003 0.002 0.002 0.003 0.004 0.002 0.003 0.003 0.003 0.002 0.003 0.003 0.001 0.004 0.002 0.003 0.003 0.003 0.003 0.004 0.003
Yb
0.007 0.006 0.006 0.007 0.005 0.005 0.004 0.007 0.004 0.009 0.005 0.007 0.007 0.009 0.005 0.007 0.007 0.005 0.009 0.006 0.006 0.005 0.006 0.006 0.006 0.007
Lu
0.003 0.006 0.006 0.003 0.005 0.005 0.004 0.003 0.005 0.002 0.007 0.003 0.001 0.004 0.007 0.003 0.001 0.003 0.004 0.004 0.004 0.005 0.004 0.007 0.004 0.002
Fe
2+
0.000
0.000
0.001
0.000
0.000
0.000
0.000
0.000
0.000
0.002
0.002
0.000
0.000
0.006
0.002
0.000
0.000
0.000
0.000
0.002
0.000
0.000
0.000
0.011
0.006
0.029
S
0.003 0.003 0.004 0.051 0.044 0.003 0.005 0.011 0.041 0.003 0.003 0.005 0.003 0.001 0.003 0.005 0.003 0.003 0.003 0.002 0.004 0.003 0.004 0.002 0.003 0.002
Ca
0.224 0.180 0.198 0.242 0.233 0.080 0.080 0.192 0.186 0.191 0.101 0.116 0.149 0.207 0.101 0.116 0.149 0.083 0.170 0.113 0.116 0.128 0.147 0.115 0.135 0.081
Sr
0.000 0.002 0.001 0.003 0.003 0.000 0.001 0.001 0.000 0.003 0.000 0.002 0.001 0.000 0.000 0.002 0.001 0.000 0.001 0.003 0.002 0.001 0.000 0.001 0.001 0.000
Al
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 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.000
Σcat.
8.024 8.040 8.028 8.040 8.037 8.036 8.041 8.035 8.042 8.023 8.015 8.019 8.023 8.031 8.015 8.019 8.023 8.023 8.036 8.025 8.012 8.020 8.018 8.026 8.027 8.025
Age (Ma)
353 344 340 348 358 266 272 340 346 247 247 352 271 255 247 352 271 257 236 255 371 274 262 261 253 252
2 sd
17.4 26.3 22.7 21.9 22.5 30.8 35.2 16.3 23.5 21.7 44.1 28.2 24.4 15.8 44.1 28.2 24.4 30.3 24.2 40.2 25.8 27.2 23.8 23.5 23.5 25.7
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, OCTOBER 2014, 65, 5
Electronic supplement
VOZÁROVÁ et al.: Provenance of Permian Malužiná Formation sandstones (Hronicum, Western Carpathians): evidence from monazite geochronology
Appendix 1
Table 3: Continued.
Sample
23-VD
Point
1/1 1/2 1/3 2/1 2/2 3/1 3/2 3/3 4/1 4/2 4/3 4/4 4/5 4/6 4/7 5/1 5/2 5/3 5/4 5/5 5/6 5/7 5/8 5/9 6/1 6/2 6/3 6/4 6/5 7/1 7/2 7/3
C. C. C. C. C. C. C. C. C. C. C. C. C. C. C. C. C. C. C. C. C. C. C. C. C. C. C. C. C. C. C. C.
P
2
O
5
28.73 28.98 29.03 30.85 30.81 29.85 29.85 30.12 30.09 30.12 30.08 29.89 29.92 29.65 29.82 27.16 30.34 30.31 28.85 28.84 30.03 29.94 27.84 27.64 30.67 30.90 31.04 30.98 31.04 31.38 31.33 30.65
As
2
O
5
0.15
0.14
0.14
0.13
0.13
0.14
0.15
0.14
0.13
0.13
0.14
0.14
0.14
0.12
0.14
0.14
0.13
0.14
0.14
0.14
0.14
0.14
0.13
0.14
0.13
0.14
0.14
0.13
0.13
0.13
0.12
0.14
SiO
2
0.66
0.65
0.75
0.35
0.36
0.25
0.26
0.26
0.18
0.22
0.28
0.26
0.26
0.32
0.30
1.86
0.18
0.17
0.86
0.87
0.19
0.18
1.53
1.84
0.20
0.15
0.15
0.23
0.16
0.22
0.24
0.34
ThO
2
6.07
7.18
6.81
4.61
4.43
3.89
3.73
3.07
3.43
3.50
3.97
3.16
3.42
4.18
3.66 10.19
4.82
4.88
5.80
5.78
4.81
5.07
9.76
9.91
3.76
3.88
3.96
3.74
3.86
3.72
3.78
3.96
PbO
0.10
0.11
0.11
0.11
0.10
0.10
0.10
0.08
0.09
0.09
0.10
0.08
0.09
0.12
0.11
0.16
0.13
0.13
0.10
0.10
0.19
0.14
0.15
0.18
0.08
0.08
0.08
0.09
0.08
0.12
0.11
0.12
UO
2
0.16
0.22
0.18
0.81
0.71
0.86
0.83
0.70
0.81
0.78
0.94
0.79
0.82
1.02
1.09
0.35
1.28
1.25
0.32
0.34
2.43
1.39
0.39
0.74
0.53
0.51
0.55
0.55
0.52
1.31
1.15
1.28
Y
2
O
3
0.44
0.90
0.42
2.26
2.00
0.86
0.76
0.89
1.95
1.76
0.84
0.67
0.69
0.80
0.77
1.20
2.37
2.61
1.39
1.42
2.23
2.44
1.65
1.65
2.73
2.88
2.96
2.69
2.81
2.84
2.66
1.31
La
2
O
3
14.85 12.89 14.21 13.54 13.60 13.42 13.64 13.83 12.68 12.79 13.08 13.71 13.25 12.94 13.07 12.11 13.07 12.53 13.18 12.96 13.21 12.99 12.01 12.16 12.28 12.24 12.09 12.20 12.51 13.32 13.56 14.26
Ce
2
O
3
30.17 29.15 30.03 28.49 28.76 28.77 29.32 29.54 27.60 28.04 28.70 29.18 28.75 28.11 28.69 26.28 27.90 27.11 28.61 28.29 27.72 27.36 26.06 25.79 27.06 27.03 27.04 27.55 27.10 27.53 27.76 28.63
Pr
2
O
3
3.34
3.33
3.40
3.26
3.30
3.54
3.41
3.45
3.34
3.34
3.55
3.43
3.46
3.33
3.34
3.17
3.22
3.21
3.39
3.31
3.13
3.16
3.17
3.17
3.35
3.36
3.34
3.38
3.37
3.24
3.23
3.37
Nd
2
O
3
12.09 12.50 11.84 12.27 12.22 13.45 13.28 13.57 13.35 13.33 13.45 13.66 13.79 13.46 13.52 12.47 11.94 12.23 12.82 12.66 11.40 11.88 12.42 12.26 13.35 13.41 13.28 13.34 13.56 11.97 12.01 12.51
Sm
2
O
3
1.62
2.01
1.55
2.08
2.12
2.48
2.41
2.47
2.70
2.72
2.69
2.65
2.64
2.67
2.72
2.38
2.15
2.28
2.32
2.33
1.87
2.14
2.52
2.18
2.72
2.80
2.81
2.83
2.80
2.37
2.32
2.25
Eu
2
O
3
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
Gd
2
O
3
0.97
1.17
0.86
1.48
1.45
1.88
1.80
1.86
2.36
2.19
1.87
1.94
1.90
1.98
1.90
1.63
1.59
1.74
1.59
1.61
1.36
1.63
1.77
1.55
2.14
2.19
2.29
2.13
2.23
1.93
1.92
1.53
Tb
2
O
3
0.00
0.08
0.01
0.14
0.11
0.09
0.11
0.12
0.20
0.19
0.13
0.12
0.12
0.19
0.08
0.08
0.15
0.17
0.11
0.10
0.11
0.14
0.10
0.12
0.16
0.17
0.24
0.20
0.14
0.14
0.22
0.08
Dy
2
O
3
0.16
0.25
0.15
0.62
0.60
0.41
0.39
0.48
0.85
0.77
0.47
0.36
0.39
0.42
0.42
0.42
0.66
0.79
0.41
0.47
0.52
0.67
0.51
0.47
0.87
0.90
0.92
0.85
0.92
0.83
0.90
0.48
Ho
2
O
3
0.02
0.06
0.01
0.06
0.07
0.00
0.05
0.00
0.07
0.08
0.03
0.06
bdl.
0.02
0.04
0.04
0.01
0.08
0.01
0.11
0.09
0.07
0.07
0.03
0.09
0.04
0.08
0.07
0.05
0.02
0.06
0.02
Er
2
O
3
0.36
0.35
0.31
0.47
0.47
0.38
0.30
0.31
0.41
0.41
0.34
0.31
0.38
0.36
0.33
0.41
0.43
0.51
0.43
0.37
0.45
0.45
0.43
0.44
0.47
0.50
0.46
0.45
0.48
0.52
0.45
0.36
Tm
2
O
3
0.06
0.09
0.11
0.06
0.09
0.07
0.07
0.06
0.08
0.08
0.11
0.06
0.05
0.06
0.09
0.10
0.08
0.08
0.09
0.06
0.11
0.10
0.08
0.08
0.15
0.11
0.07
0.06
0.08
0.04
0.09
0.09
Yb
2
O
3
0.14
0.11
0.12
0.19
0.17
0.09
0.10
0.13
0.09
0.11
0.15
0.08
0.12
0.09
0.14
0.11
0.14
0.18
0.14
0.15
0.12
0.13
0.16
0.13
0.15
0.11
0.17
0.14
0.15
0.18
0.16
0.14
Lu
2
O
3
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
FeO
0.06
0.05
0.02
0.14
0.22
0.05
0.14
0.12
0.07
0.03
bdl.
bdl.
bdl.
0.00
0.05
0.06
bdl.
0.01
bdl.
bdl.
0.08
bdl.
bdl.
0.11
0.30
0.13
0.14
0.14
0.11
0.17
0.13
0.14
SO
3
0.02
0.06
0.03
0.02
0.05
0.03
0.03
0.02
0.01
0.01
0.03
0.02
0.02
0.02
0.02
0.19
0.01
0.02
0.26
0.23
0.02
0.01
0.17
0.13
0.04
0.02
0.02
0.03
0.03
0.03
0.02
0.03
CaO
0.87
1.18
0.99
0.96
0.94
0.96
0.88
0.74
0.87
0.86
0.96
0.75
0.80
0.98
0.88
0.92
1.28
1.27
0.92
0.90
1.48
1.33
1.05
1.00
0.94
0.90
0.93
0.89
0.91
1.02
0.99
0.99
SrO
0.03
0.02
0.01
0.02
0.07
0.01
0.00
0.01
0.01
0.03
0.02
0.02
0.00
bdl.
0.01
0.03
0.01
0.01
0.04
0.03
0.01
0.01
0.03
0.03
0.02
0.03
0.03
0.02
0.01
0.04
0.01
0.02
Al
2
O
3
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
bdl.
0.03
bdl.
bdl.
0.01
bdl.
0.00
bdl.
0.04
Total
101.06 101.49 101.09 102.93 102.77 101.58 101.60 101.98 101.36 101.58 101.93 101.34 100.99 100.86 101.20 101.47 101.90 101.70 101.76 101.06 101.71 101.37 102.00 101.74 102.23 102.48 102.79 102.71 103.04 103.07 103.21 102.76
P
3.840 3.844 3.858 3.953 3.953 3.927 3.926 3.938 3.946 3.944 3.937 3.940 3.949 3.929 3.935 3.649 3.945 3.947 3.803 3.818 3.926 3.929 3.704 3.680 3.954 3.971 3.974 3.969 3.970 3.987 3.983 3.948
Si
0.104 0.102 0.117 0.054 0.054 0.040 0.040 0.040 0.028 0.034 0.043 0.040 0.040 0.050 0.046 0.296 0.027 0.026 0.134 0.136 0.030 0.028 0.240 0.289 0.030 0.022 0.023 0.034 0.024 0.033 0.036 0.052
As
0.012 0.012 0.012 0.010 0.010 0.011 0.012 0.012 0.011 0.010 0.011 0.012 0.011 0.010 0.011 0.011 0.010 0.011 0.012 0.011 0.012 0.011 0.011 0.012 0.010 0.011 0.011 0.010 0.010 0.010 0.010 0.011
Th
0.218 0.256 0.243 0.159 0.153 0.138 0.132 0.108 0.121 0.123 0.140 0.112 0.121 0.149 0.130 0.368 0.169 0.171 0.205 0.206 0.169 0.179 0.349 0.355 0.130 0.134 0.136 0.129 0.133 0.127 0.129 0.137
U
0.006 0.008 0.006 0.027 0.024 0.030 0.029 0.024 0.028 0.027 0.032 0.027 0.028 0.036 0.038 0.012 0.044 0.043 0.011 0.012 0.083 0.048 0.014 0.026 0.018 0.017 0.019 0.019 0.018 0.044 0.039 0.043
Pb
0.004 0.005 0.005 0.004 0.004 0.004 0.004 0.003 0.004 0.004 0.004 0.003 0.004 0.005 0.005 0.007 0.005 0.005 0.004 0.004 0.008 0.006 0.006 0.008 0.003 0.003 0.003 0.003 0.003 0.005 0.004 0.005
Y
0.037 0.075 0.035 0.182 0.162 0.071 0.063 0.073 0.160 0.145 0.069 0.055 0.057 0.067 0.064 0.101 0.194 0.214 0.115 0.118 0.183 0.201 0.138 0.138 0.221 0.233 0.239 0.217 0.226 0.227 0.213 0.106
La
0.865 0.745 0.822 0.756 0.760 0.769 0.782 0.788 0.724 0.730 0.746 0.787 0.762 0.747 0.751 0.709 0.741 0.711 0.757 0.747 0.753 0.743 0.696 0.705 0.690 0.686 0.675 0.681 0.697 0.737 0.751 0.800
Ce
1.744 1.672 1.725 1.579 1.595 1.637 1.668 1.670 1.565 1.588 1.625 1.663 1.641 1.611 1.637 1.527 1.569 1.527 1.631 1.620 1.567 1.553 1.500 1.485 1.509 1.502 1.497 1.526 1.498 1.513 1.526 1.595
Pr
0.192 0.190 0.195 0.180 0.182 0.201 0.193 0.194 0.189 0.188 0.200 0.194 0.196 0.190 0.190 0.183 0.180 0.180 0.192 0.189 0.176 0.179 0.181 0.182 0.186 0.186 0.184 0.187 0.185 0.177 0.176 0.187
Nd
0.682 0.700 0.664 0.663 0.661 0.747 0.737 0.749 0.739 0.736 0.743 0.760 0.768 0.752 0.753 0.707 0.655 0.671 0.713 0.707 0.629 0.658 0.697 0.688 0.726 0.727 0.717 0.721 0.731 0.641 0.644 0.680
Sm
0.088 0.109 0.084 0.109 0.111 0.133 0.129 0.132 0.145 0.145 0.144 0.142 0.142 0.144 0.147 0.131 0.114 0.121 0.125 0.126 0.100 0.115 0.137 0.118 0.143 0.147 0.147 0.148 0.146 0.123 0.120 0.118
Eu
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 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 0.000 0.000 0.000 0.000
Gd
0.051 0.061 0.045 0.074 0.073 0.097 0.093 0.095 0.121 0.112 0.096 0.100 0.098 0.103 0.098 0.086 0.081 0.089 0.082 0.083 0.070 0.084 0.092 0.081 0.108 0.110 0.115 0.107 0.112 0.096 0.096 0.077
Tb
0.000 0.004 0.001 0.007 0.006 0.005 0.005 0.006 0.010 0.010 0.007 0.006 0.006 0.010 0.004 0.004 0.007 0.009 0.005 0.005 0.006 0.007 0.005 0.006 0.008 0.009 0.012 0.010 0.007 0.007 0.011 0.004
Dy
0.008 0.013 0.007 0.030 0.029 0.021 0.019 0.024 0.042 0.039 0.023 0.018 0.019 0.021 0.021 0.022 0.033 0.039 0.021 0.024 0.026 0.033 0.026 0.024 0.043 0.044 0.045 0.042 0.045 0.040 0.044 0.024
Ho
0.001 0.003 0.001 0.003 0.003 0.000 0.003 0.000 0.003 0.004 0.001 0.003 0.000 0.001 0.002 0.002 0.001 0.004 0.000 0.005 0.004 0.004 0.003 0.001 0.004 0.002 0.004 0.003 0.002 0.001 0.003 0.001
Er
0.018 0.017 0.015 0.022 0.022 0.018 0.015 0.015 0.020 0.020 0.017 0.015 0.019 0.017 0.016 0.021 0.021 0.025 0.021 0.018 0.022 0.022 0.021 0.022 0.022 0.024 0.022 0.022 0.023 0.025 0.021 0.017
Tm
0.003 0.004 0.006 0.003 0.004 0.004 0.003 0.003 0.004 0.004 0.005 0.003 0.003 0.003 0.004 0.005 0.004 0.004 0.004 0.003 0.005 0.005 0.004 0.004 0.007 0.005 0.003 0.003 0.004 0.002 0.004 0.004
Yb
0.007 0.005 0.006 0.009 0.008 0.004 0.005 0.006 0.004 0.005 0.007 0.004 0.006 0.004 0.007 0.005 0.007 0.008 0.007 0.007 0.006 0.006 0.008 0.006 0.007 0.005 0.008 0.007 0.007 0.008 0.007 0.007
Lu
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 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 0.000 0.000 0.000 0.000
Fe
2+
0.008 0.006 0.002 0.018 0.028 0.006 0.018 0.016 0.009 0.004 0.000 0.000 0.000 0.000 0.006 0.008 0.000 0.001 0.000 0.000 0.011 0.000 0.000 0.015 0.039 0.017 0.018 0.018 0.014 0.022 0.016 0.018
S
0.003 0.007 0.003 0.003 0.006 0.004 0.004 0.002 0.001 0.001 0.003 0.002 0.002 0.002 0.002 0.022 0.001 0.002 0.030 0.027 0.003 0.001 0.020 0.016 0.005 0.003 0.002 0.003 0.003 0.004 0.002 0.003
Ca
0.148 0.199 0.166 0.156 0.152 0.161 0.147 0.122 0.145 0.142 0.159 0.125 0.134 0.165 0.148 0.157 0.211 0.210 0.154 0.151 0.244 0.221 0.177 0.168 0.154 0.146 0.150 0.145 0.148 0.164 0.159 0.161
Sr
0.002 0.001 0.001 0.002 0.006 0.001 0.000 0.001 0.001 0.003 0.001 0.002 0.000 0.000 0.001 0.003 0.001 0.001 0.004 0.003 0.001 0.001 0.003 0.003 0.002 0.003 0.002 0.002 0.001 0.003 0.001 0.001
Al
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 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.005 0.000 0.000 0.001 0.000 0.000 0.000 0.008
Σcat.
8.040 8.037 8.019 8.002 8.005 8.026 8.027 8.021 8.021 8.019 8.014 8.014 8.007 8.017 8.016 8.036 8.020 8.018 8.030 8.021 8.032 8.030 8.032 8.031 8.025 8.007 8.006 8.006 8.007 7.995 7.995 8.009
Age
(Ma) 355 347 369 352 369 360 365 351 344 340 353 345 364 365 355 348 351 341 363 349 345 351 331 352 345 349 342 368 342 351 349 343
2 sd
25.8 21.8 23.4 23.9 25.5 25.3 25.9 30.9 27.3 27.4 24.0 28.8 27.3 22.6 23.4 16.0 19.1 19.3 25.2 24.8 14.1 18.1 16.1 14.9 30.7 30.1 29.2 30.5 30.0 21.5 22.8 20.9
ii
Article
in
Proof
G
G
G
G
GEOL
EOL
EOL
EOL
EOLOGICA CARPA
OGICA CARPA
OGICA CARPA
OGICA CARPA
OGICA CARPATHICA
THICA
THICA
THICA
THICA
, OCTOBER 2014, 65, 5
Electronic supplement
VOZÁROVÁ et al.: Provenance of Permian Malužiná Formation sandstones (Hronicum, Western Carpathians): evidence from monazite geochronology
Appendix 1
Table 3: Continued.
iii
Sample
31-VD 32-VD
33-VD
22-VD
Point 1/1 1/2 2/1 2/2 3/1 3/2 1/1 2/1 1/1 2/1 2/1 2/2 2/3 4/1 4/4 4/5 5/1
C. C. C. C. C. C. C. C. C. C. C. C. C. P. P. P. P.
P
2
O
5
31.08 29.92 30.26 29.94 29.74 29.78 29.94 29.74 29.32 29.54 29.96 30.21 30.19 29.12 29.01 28.45 28.20
As
2
O
5
0.08 0.09 0.08 0.09 0.09 0.09 0.10 0.09 0.08 0.09 0.13 0.14 0.13 0.32 0.49 0.64 0.51
SiO
2
0.29 0.37 0.23 0.26 0.43 0.43 0.41 0.50 0.40 0.44 0.28 0.25 0.20 0.81 0.74 0.55 0.40
ThO
2
2.70 4.04 2.54 3.22 3.86 3.86 4.05 6.57 5.08 2.11 3.27 3.41 3.60 6.50 3.72 3.67 2.59
PbO
0.06 0.08 0.06 0.09 0.06 0.06 0.07 0.12 0.10 0.07 0.09 0.09 0.10 0.07 0.04 0.04 0.04
UO
2
0.57 0.68 0.52 0.58 0.32 0.31 0.29 0.42 0.68 0.68 0.93 0.90 0.84 0.11 0.05 0.07 0.37
Y
2
O
3
1.70 1.10 1.83 1.77 1.83 1.85 1.28 1.55 1.88 0.69 2.37 2.07 1.84 0.25 0.18 0.19 0.98
La
2
O
3
13.55 13.75 13.35 13.05 13.43 13.57 14.93 12.25 12.12 13.52 12.57 12.76 12.88 15.08 17.07 16.59 14.65
Ce
2
O
3
28.67 29.12 28.27 27.61 28.69 28.71 29.70 27.65 27.09 29.64 27.66 27.81 28.33 31.43 32.69 32.65 29.12
Pr
2
O
3
3.46 3.36 3.47 3.28 3.38 3.41 3.30 3.39 3.32 3.63 3.34 3.35 3.51 3.22 3.26 3.19 3.26
Nd
2
O
3
13.50 13.10 14.09 13.73 12.91 12.85 12.51 12.94 13.44 14.38 13.31 13.38 13.29 10.31 11.03 10.31 11.80
Sm
2
O
3
2.51 2.28 2.92 2.87 2.54 2.57 1.87 2.36 2.86 2.76 2.93 2.93 2.88 1.50 1.53 1.53 2.32
Eu
2
O
3
bdl. bdl. bdl. bdl. bdl. bdl. bdl. bdl. bdl. bdl. 0.16 0.12 0.11 0.37 0.37 0.43
0.26
Gd
2
O
3
1.87 1.69 2.10 2.20 1.94 1.83 1.24 1.62 2.05 2.06 2.09 1.97 1.80 0.32 0.31 0.32 1.02
Tb
2
O
3
0.16 0.14 0.19 0.14 0.12 0.17 0.07 0.11 0.24 0.10 0.25 0.21 0.17 0.05 0.05 0.02 0.10
Dy
2
O
3
0.64 0.37 0.71 0.71 0.67 0.71 0.38 0.42 0.69 0.34 1.01 0.86 0.83 0.05 0.13 0.12 0.42
Ho
2
O
3
0.05 0.04 0.12 0.10 0.04 0.05 0.03 0.03 0.06 0.01 0.07 0.10 0.07 bdl. bdl. 0.01 0.07
Er
2
O
3
0.43 0.30 0.43 0.40 0.37 0.42 0.35 0.40 0.45 0.31 0.37 0.34 0.30 0.33 0.30 0.26 0.32
Tm
2
O
3
0.07 0.13 0.08 0.10 0.09 0.09 0.06 0.10 0.09 0.09 0.04 0.04 0.02 0.06 0.04 0.03 0.04
Yb
2
O
3
0.10 0.11 0.15 0.15 0.10 0.17 0.11 0.12 0.14 0.13 0.10 0.13 0.13 0.11 0.12 0.09 0.09
Lu
2
O
3
bdl. bdl. bdl. bdl. bdl. bdl. bdl. bdl. bdl. bdl. 0.07 0.05 0.05 0.07 0.06 0.04
0.13
FeO
0.06 0.10 0.28 0.44 0.33 0.38 bdl. bdl. 0.07 0.30 bdl. bdl. bdl. 0.17 0.52 0.51 0.07
SO
3
0.02 0.03 0.03 0.04 0.02 0.02 0.03 0.00 0.02 0.02 0.02 0.03 0.03 0.23 0.18 0.15 0.09
CaO
0.60 0.96 0.71 0.79 0.64 0.63 1.03 1.39 1.10 0.59 0.76 0.85 0.90 1.13 0.63 0.71 0.62
SrO
0.00 0.03 0.03 0.02 0.00 bdl. 0.01 0.00 bdl. 0.01 0.00 0.01 0.01 0.40 0.22 0.25 0.06
Al
2
O
3
0.00 bdl. 0.00 0.00 bdl. bdl. bdl. bdl. 0.02 bdl. bdl. bdl. bdl. bdl. 0.01 bdl.
0.00
Total
102.18 101.81 102.46 101.58 101.62 101.97 101.76 101.75 101.30 101.52 101.79 102.02 102.20 102.01 102.75 100.83 97.53
P
3.996 3.918 3.931 3.924 3.904 3.899 3.913 3.899 3.882 3.898 3.921 3.937 3.935 3.818 3.793 3.796 3.865
Si
0.044 0.058 0.035 0.040 0.067 0.067 0.063 0.077 0.062 0.068 0.044 0.039 0.031 0.125 0.114 0.087 0.064
As
0.006 0.007 0.007 0.007 0.007 0.008 0.008 0.007 0.006 0.008 0.010 0.011 0.011 0.026 0.040 0.053 0.043
Th
0.093 0.142 0.089 0.113 0.136 0.136 0.142 0.231 0.181 0.075 0.115 0.119 0.126 0.229 0.131 0.132 0.095
U
0.019 0.023 0.018 0.020 0.011 0.011 0.010 0.014 0.024 0.023 0.032 0.031 0.029 0.004 0.002 0.002 0.013
Pb
0.002 0.003 0.003 0.004 0.003 0.003 0.003 0.005 0.004 0.003 0.004 0.004 0.004 0.003 0.002 0.002 0.002
Y
0.137 0.091 0.150 0.145 0.151 0.152 0.105 0.127 0.156 0.057 0.195 0.169 0.151 0.020 0.015 0.016 0.084
La
0.759 0.785 0.755 0.745 0.768 0.774 0.850 0.699 0.699 0.777 0.717 0.724 0.731 0.862 0.972 0.964 0.875
Ce
1.594 1.649 1.588 1.565 1.628 1.626 1.678 1.567 1.551 1.691 1.565 1.567 1.596 1.782 1.848 1.884 1.726
Pr
0.191 0.190 0.194 0.185 0.191 0.192 0.185 0.191 0.189 0.206 0.188 0.188 0.197 0.182 0.183 0.183 0.192
Nd
0.732 0.724 0.772 0.759 0.715 0.710 0.690 0.715 0.750 0.800 0.735 0.736 0.730 0.570 0.608 0.580 0.682
Sm
0.131 0.122 0.155 0.153 0.136 0.137 0.100 0.126 0.154 0.149 0.157 0.156 0.153 0.080 0.081 0.083 0.130
Eu
0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.008 0.006 0.006 0.020 0.020 0.023 0.015
Gd
0.094 0.087 0.107 0.113 0.100 0.094 0.063 0.083 0.106 0.106 0.107 0.100 0.092 0.016 0.016 0.017 0.055
Tb
0.008 0.007 0.010 0.007 0.006 0.009 0.004 0.006 0.012 0.005 0.013 0.011 0.009 0.003 0.002 0.001 0.005
Dy
0.032 0.018 0.035 0.036 0.034 0.035 0.019 0.021 0.035 0.017 0.050 0.043 0.041 0.003 0.006 0.006 0.022
Ho
0.003 0.002 0.006 0.005 0.002 0.002 0.001 0.001 0.003 0.001 0.003 0.005 0.003 0.000 0.000 0.000 0.004
Er
0.021 0.014 0.021 0.019 0.018 0.021 0.017 0.019 0.022 0.015 0.018 0.017 0.014 0.016 0.014 0.013 0.016
Tm
0.003 0.006 0.004 0.005 0.004 0.004 0.003 0.005 0.004 0.004 0.002 0.002 0.001 0.003 0.002 0.001 0.002
Yb
0.005 0.005 0.007 0.007 0.005 0.008 0.005 0.006 0.007 0.006 0.005 0.006 0.006 0.005 0.005 0.004 0.004
Lu
0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.003 0.002 0.002 0.003 0.003 0.002 0.007
Fe
2+
0.008 0.013 0.037 0.057 0.043 0.049 0.000 0.000 0.009 0.039 0.000 0.000 0.000 0.022 0.068 0.067 0.009
S
0.002 0.004 0.004 0.005 0.002 0.002 0.004 0.000 0.002 0.003 0.003 0.003 0.003 0.027 0.021 0.018 0.010
Ca
0.098 0.159 0.116 0.130 0.106 0.105 0.171 0.230 0.185 0.098 0.126 0.140 0.149 0.188 0.104 0.119 0.108
Sr
0.000 0.003 0.003 0.001 0.000 0.000 0.001 0.000 0.000 0.001 0.000 0.001 0.001 0.036 0.020 0.023 0.006
Al
0.000 0.000 0.000 0.001 0.000 0.000 0.000 0.000 0.004 0.000 0.000 0.000 0.000 0.000 0.003 0.000 0.000
Σcat.
7.980 8.031 8.043 8.048 8.036 8.042 8.035 8.033 8.049 8.051 8.022 8.017 8.022 8.041 8.072 8.078 8.034
Age (Ma)
311 323 345 401 315 319 358 365 332 391 345 355 359 246 229 254 256
2 sd
35.4 26.8 38.3 32.9 33.8 33.6 33.5 22.0 31.4 37.9 24.3 24.6 24.7 21.8 37.2 37.2 38.5