GEOLOGICA CARPATHICA
, JUNE 2019, 70, 3, 222–240
doi: 10.2478/geoca-2019-0013
www.geologicacarpathica.com
Geochronology and Sr–Nd–Hf isotope constraints
on the petrogenesis of teschenites from the type-locality
in the Outer Western Carpathians
IRENA BRUNARSKA and ROBERT ANCZKIEWICZ
Institute of Geological Sciences, Polish Academy of Sciences, Kraków Research Centre, Senacka 1, 31-002 Kraków, Poland;
ndanczki@cyfronet.pl
(Manuscript received September 21, 2018; accepted in revised form May 9, 2019)
Abstract: The Teschenite Association Rocks (TAR) in the Outer Western Carpathian (OWC) flysch form a classic suite
of alkaline intrusions where teschenite and picrite were first defined. They represent continental intraplate volcanism that
produced a wide range of melano- to mesocratic rocks emplaced during the Early Cretaceous rifting within the southern
margin of the European Plate. Geochemical modelling indicates that they may be a product of ~2–5 % partial melting of
the metasomatised, asthenospheric mantle. The variations in REE (low / heavy REE content, La
N
/Yb
N
= 11–34) are consistent
with deep melting of garnet peridotite. Initial ε(Nd)
i
= 5.0–6.3 and ε(Hf)
i
= 4.9–10.0 preclude the significant mature crust
involvement. Instead, a linear array formed by the
143
Nd/
144
Nd and
176
Hf/
177
Hf isotopic ratios points to a genesis from
the mixed, HIMU–OIB source with the more depleted, MORB-type component. Mantle metasomatism was most likely
caused by the Variscan subduction–collision processes as indicated by the depleted mantle Nd model ages. The isotope
and trace element ratios of the TAR resemble the European Asthenospheric Reservoir (EAR) — the common mantle
end-member for the widespread Cenozoic volcanic rocks in Europe. This confirms a long-term existence of the EAR
mantle component beneath the Central Europe, at least since the Early Cretaceous. In situ laser-ablation ICP-MS U–Pb
dating of titanite indicates short duration of mafic alkaline magmatism in the OWC, lasting from 123.7 ± 2.1 to 117.9 ± 1.8 Ma.
Emplacement of the TAR is correlated with the maximum lithospheric thinning that triggered adiabatic decompression
and partial melting of the upwelling asthenospheric mantle. Magmatism ceased most likely due to transition to
the dominantly compressive regime associated with the major stress field reorganization directly preceding the Carpathian–
Alpine Orogeny.
Keywords: mafic alkaline magmatism, teschenite, picrite, Outer Western Carpathians, laser ablation U–Pb titanite dating.
Introduction
The Teschenite Association Rocks (TAR) in the Outer Western
Carpathians (OWC) at the Polish–Czech border belong to
rather numerous manifestations of the Cretaceous–Cenozoic
mafic alkaline volcanism in Europe (Rock 1982; Wilson &
Downes 1991; Rossy et al. 1992; Cebriá & Wilson 1995;
Spišiak & Balogh 2002; Harangi et al. 2003; Miranda et al.
2009; Spišiak et al. 2011; Matýsek et al. 2018). The TAR form
a classic suite of melano- to mesocratic alkaline intrusions
emplaced within the OWC flysch named teschenites by
Hohenegger (1861). Tschermak (1866) coined the term picrite
for olivine-bearing teschenites distinguishing them from
the dominant olivine-free teschenites. Rosenbusch (1887) fur-
ther classified teschenites as analcime-bearing essexites and
analcime-free theralites. The subsequent studies distinguished
many more petrographic varieties of the TAR which resulted
in further discoveries of teschenite variations (Smulikowski
1929, 1980; Mahmood 1973; Kudělásková 1987; Hovorka &
Spišiak 1988; Narębski 1990; Dostal & Owen 1998; Harangi
et al. 2003; Włodyka 2010; Matýsek et al. 2018). According to
QAPF classification, the TAR correspond to analcime gabbro
(LeMaitre et al. 1989).
Rare petrogenetic studies linked the TAR to Jurassic–Early
Cretaceous rifting within the southern margin of the European
Plate and partial melting of HIMU (high
238
U/
204
Pb)-type
mantle source (Dostal & Owen 1998; Harangi et al. 2003).
Although there is some uncertainty about the exact timing and
duration of the TAR magmatism, stratigraphic criteria and
radiometric dating broadly constrain the emplacement time
between Valanginian and Cenomanian (Kudělásková 1987;
Lucińska-Anczkiewicz et al. 2002; Grabowski et al. 2003;
Harangi et al. 2003; Szopa et al. 2014). Thus, the TAR provide
a valuable insight into mantle composition, geodynamics and
lithospheric processes in the complex paleo-tectonic setting
directly preceding formation of the Alpine–Carpathian
Orogen.
In this study we review previously published geochemical
and isotopic data, and further constrain composition, geochro-
nology and likely petrogenesis of the Teschenite Association
Rocks. Besides the previously conducted Sr and Nd isotope
studies, we also apply Hf isotope analyses which provide
a new insight into the genesis of TAR. We give detailed
charac teristics of all main petrographic types along with geo-
chemical modelling of partial melting and magma differentia-
tion processes. Additionally, our in situ U–Pb titanite dating
223
TESCHENITES FROM THE TYPE-LOCALITY IN THE OUTER WESTERN CARPATHIANS
GEOLOGICA CARPATHICA
, 2019, 70, 3, 222–240
results demonstrate short duration of the TAR emplacement
during the early Aptian.
Regional geology
The current structure of the OWC was shaped mainly by
the Early/Middle Miocene collision of the Alcapa Block with
the southern margin of the European Plate during which pre-
dominantly Late Jurassic to Early Miocene shelf and deep
water flysch deposits with minor carbonates were thrust north-
ward over the Miocene molasse deposits of the Carpathian
foredeep (Nemčok et al. 1989; Rögl 1996; Sperner et al. 2002).
The suture zone is correlated with the Pieniny Klippen Belt
(PKB), which is a narrow, E–W trending zone formed mainly
by the Triassic to Oligocene sediments, predominantly carbo-
nates with subordinate fragments of ophiolites deformed in
a transpressive setting due to oblique, generally south directed,
subduction of the oceanic crust (Birkenmajer 1977, 1986;
Nemčok et al. 1989). The PKB separates paleo-accretionary
prism of the OWC to the north from the southerly units of
the Internal Carpathian chain (Fig. 1a).
Igneous rocks in the OWC are scarce and volumetrically
minor. Rare example of continental intraplate magmatic acti-
vity is represented by the TAR whose occurrence is limited to
the western part of the Silesian Nappe composed of the Upper
Jurassic to Miocene, predominantly flysch sediments with
subordinate volcaniclastic rocks (Fig. 1b).
The vast majority of the TAR in Poland (Silesia region)
occurs in the Valanginian–Hauterivian Upper Cieszyn Beds
comprising mainly marls and shales. The Moravian TAR,
in the Czech Republic, occur in the Upper Hauterivian–
Barremian sandstones and conglomerates of the Těšín–
Hradiště Beds and, very rarely, in the Upper Cieszyn Beds and
Cieszyn Limestones (Oszczypko 2006).
Teschenites form centimetres to tens of meters thick
hypabyssal intrusions (predominantly sills), rarely volcanic
flows. They display numerous petrographic and geochemical
types ranging from ultrabasic picrites to intermediate tesche-
nites and syenites. Although the radiometric dating results
broadly confirm their Early Cretaceous age deduced from
the stratigraphic data, they differ substantially when it comes
to exact timing and duration of emplacement. The first dating
using Ar–Ar method on kaersutite gave ages indicating short
duration of magmatism from 122.3 ± 3.2 to 120.4 ± 2.6 Ma
(Lucińska-Anczkiewicz et al. 2002). The subsequent K–Ar and
U–Pb dating resulted in highly scattered ages suggesting much
longer time of the TAR emplacement during Valanginian to
Barremian–Aptian (Grabowski et al. 2003; Harangi et al.
2003; Szopa et al. 2014; Matýsek et al. 2018).
Sampling and methods
We present the analyses of 21 TAR samples from 10 loca-
tions in the Czech Republic and 5 locations in Poland (Table 1,
Fig. 1b). The whole-rock powders and the heavy-mineral
separates were prepared by commonly used techniques of
crushing, sieving, magnetic and the heavy liquids separation.
About 2–10 kg of rock was first crushed to gravel size in a jaw
crusher and then split until 50–100 g of representative whole-
rock portion was achieved. This was powdered in an auto-
mated agate mortar and subsequently used for geochemical
and isotopic analyses. The remaining part of a sample was
further crushed to a fraction < 315 µm from which heavy
minerals were separated using tetrabromethane followed by
diiodomethane
. The final steps involved magnetic separation
and handpicking under the stereo microscope.
Whole-rock geochemistry
Geochemical analyses were carried out commercially at
the Acme Analytical Laboratories in Canada (http://acmelab.
com). Samples were first fused with lithium tetraborate and
subsequently brought into solution by digestion in nitric acid.
Abundance of major elements was determined using ICP-ES
while minor and trace elements were measured using ICP-MS
(package LF200). Exceptions were Mo, Cu, Pb, Zn and Ni
which were first digested in 1:1:1 HNO
3
: HCl : H
2
O mixture
and measured by ICP-MS.
Mineral chemistry
Chemical composition of the selected minerals was deter-
mined using the Cameca SX-100 electron microprobe at
the Faculty of Geology, University of Warsaw. The natural and
synthetic standards used during analyses were: albite, apatite,
diopside, orthoclase, rutile, rhodonite, zircon, barite, tugtupite,
Fe
2
O
3
, Cr
2
O
3
, La-glass, Pr-glass, CeP
5
O
14
, Nb, NiO, V
2
O
5
,
ThO
2
, UO
2
, HfO
2
. We applied 15 kV accelerating voltage,
10–20 nA sample current and 1–5 µm beam diameter (larger
beam size was applied to mica and feldspar). Integration
time at the peak was 10 s and the background was measured
for 5 s. The ZAF method was used for correcting the matrix
effects.
U–Pb titanite geochronology
Geochronological analyses were carried out in Kraków
Research Centre, Institute of Geological Sciences, Polish
Academy of Sciences.
In situ U–Pb titanite dating was performed using an excimer
laser (ArF) RESOlution M-50 by Resonetics (now Applied
Spectra) equipped with a large format, dual-volume sample
cell S155 coupled with the ICP-MS XSeriesII by ThermoFisher.
Titanite crystals were mounted in an epoxy resin and polished.
Prior to analyses, a mount was cleaned using acetone, fol-
lowed by 1N nitric acid and ultra-pure water. Ablation took
place in pure He which was mixed in an ablation funnel with
Ar nebulizer gas. Downstream, nitrogen was added to enhance
sensitivity of the ICP-MS. Before entering ICP source, aerosol
passed through a signal smoothing manifold. Basic tuning of
224
BRUNARSKA and ANCZKIEWICZ
GEOLOGICA CARPATHICA
, 2019, 70, 3, 222–240
N
0
100 km
Inner Alpine-Carpathian-Dinarides belt
Thrust fault
Strike-slip fault
Fig. 1b
European foreland
Dinarides
Outer Western Carpathians
Inner Western
Carpathians
Eastern Carpathians
Southern Carpathians
ALPS
DIN
AR
IDE
S
Adriatic Sea
BALKANS
Black Sea
PANNONIAN
BASIN
CENTRAL
EUROPEAN
PLATFORM
EASTERN
EUROPEAN
PLATFORM
Baltic Sea
Tei
ey
e-To
rn
u st
one
ss
r
q
i
z
POLAND
Kraków
300 km
Transylvanian
Basin
Apuseni
Mts.
European foreland
V
n
a
ie
n
Ba
sin
b
Danu e
a n
B si
16°
19°
22°
25°
28°
45°
46°
47°
48°
49°
50°
Pannonian Basin
Eastern Alps
ALCAP
A
TISIA
Mid-Hungarian fault zo
ne
C A R P A T
H I
A
N
S
Neogene calc-alkaline volcanic rocks
Pieniny Klippen Belt
Outer Carpathian flysch
Mollase foredeep Basin
POLAND
CZECH
REPUBLIC
SLOVAKIA
Picrite
Teschenite
Syenite
Foredeep sediments
Sub-Silesian Nappe
Cieszyn unit
Godula unit
Fore-Magura Unit
Silesian nappe
Magura Nappe
SAMPLE LOCATIONS:
CARPATHIAN FLYSCH UNITS:
Faults
Thrusts
Country
Borders
CIESZYN/
TĚŠÍN
KARVINÁ
WISŁA
ŻYWIEC
KORBIELÓW
NOVÝ JIČÍ N
WADOWICE
BIELSKO-BIAŁA
a
b
Fig. 1
N
20 km
]
Miocene deposits
Fig. 1. Simplified geological map of the Carpathian–Pannonian region (a) after Horváth (1993). Small rectangle in (a) marks the Western
Carpathian region expanded in (b) after Żytko et al. (1989) with the marked sample locations.
225
TESCHENITES FROM THE TYPE-LOCALITY IN THE OUTER WESTERN CARPATHIANS
GEOLOGICA CARPATHICA
, 2019, 70, 3, 222–240
the instrument was conducted using NIST
612 glass standard ablated in a raster mode.
Gas flows and torch position were adjusted
to maximum signal stability and oxide pro-
duction below 0.5
% (measured with
248
ThO
+
/
232
Th
+
).
We used 1014.8 ± 2.0 Ma old OLT1 titanite
(Kennedy et al. 2010) as a primary standard
and 520 ± 5 Ma titanite from Stjernøy in
Northern Norway (Pedersen et al. 1989) as
a secondary standard. Every six unknowns or
the secondary standards, two measurements
of the primary standard were carried out.
After two cleaning shots, the residual signal
was washed out for 30 s and then 35 s of gas
blank was measured which was followed by
40 s ablation. Standards and unknowns were
ablated using 40 µm spot size and the clea-
ning shots were of 60 µm dia meter. Laser
fluence of about 2 J/cm
2
was applied with
ablation frequency of 5 Hz. Sum mary of the
analytical parameters is presented in Table 2.
Data reduction was conducted using Vizual
Age_UcomPbine (Chew et al. 2014) in Iolite
v. 3.4 program (Paton et al. 2011) functioning
under IgorPro software by Wavemetrics.
Final age calculations were performed using
Isoplot 4.15 (Ludwig 2012). All intercept
ages were cal culated using common Pb composition estimated
applying model of Stacey and Kramers (1975). All reported
age errors are 2σ.
Isotope geochemistry
Isotope composition measurements of Sr, Nd and Hf were
aquired in the same laboratory as U–Pb titanite dating
described above. Sample dissolution, column chemistry and
mass spectrometric procedures are outlined in Anczkiewicz &
Anczkiewicz (2016) and references therein. Isotope ratio
measurements were conducted using multicollector induc-
tively coupled plasma mass spectrometer (MC ICP-MS)
Neptune by ThermoFisher. Instrumental mass bias of all
measured isotopic ratios was corrected using exponential law
of Russell et al. (1978). Isotopic ratios of Sr were normalized
to
87
Sr/
86
Sr = 0.1194, and initial
87
Sr/
86
Sr ratios were calculated
using decay constant λ
87Rb
= 1.3972 × 10
−11
yr
–1
(Villa et al.
2015). Repeated measurements of the SRM 987 standard over
the period of analyses gave
87
Sr/
86
Sr = 0.710258 ± 12 (n = 7).
Mass bias of Nd isotope ratios was corrected by normalization
to
146
Nd/
144
Nd = 0.7219. The JNd-1 standard yielded
143
Nd/
144
Nd
= 0.512103 ± 9 (n = 6) over a period of analyses. Constants
used for the initial ε(Nd)
i
calculations: decay constant
λ
147Sm
= 6.54×10
−12
yr
−1
(Lugmair and Marti 1978), present-day
143
Nd/
144
Nd
CHUR(0)
= 0.512637 and
147
Sm/
144
Nd
CHUR(0)
= 0.1966
(Jacobsen & Wasserburg 1980). Neodymium depleted mantle
model age T
DM
calculations followed DePaolo (1981).
Haf nium isotope ratios were normalized to
179
Hf/
177
Hf = 0.7325.
Values used for the initial ε(Hf)
i
calculations: decay con-
stant λ
176Lu
= 1.865 × 10
−11
yr
−1
(Scherer et al. 2001), present
day
176
Hf/
177
Hf
CHUR(0)
= 0.282785 and
176
Lu/
177
Hf
CHUR(0)
= 0.0336
(Bouvier et al. 2008). The JMC475 Hf standard gave
176
Hf/
177
Hf = 0.282160 ± 13 (n = 8) over the period of analyses.
TAR type
Sample GPS coordinates
Primary mineral asemblage Secondary
alterations
Picrites
CPR-1 N 49°31.584’ E 17°57.662’
Ol-Am-Bt-Cpx-(Ap)
x
CM-1
N 49°50.15’ E 18°55.11’
Cpx-Bt-Fs/Fd-(Ap)
xxxx
Teschenites CSTa-2 N 49°41.281’ E 18°16.248’
Cpx-Am-Bt-Fs/Fd-(Ap)
x
CBS-1 N 49°38.400’ E 18°21.966’
Cpx-Bt-Fs-(Ap)
x
CS-4
N 49°47.419’ E 18°53.255’
Cpx-Am-Fs/Fd-(Ap)
xx
CR-6
N 49°47.70’ E 18°38.45’
Cpx-Fs-Bt-(Ap-Ttn)
x
CP-4
N 49°43.230’ E 18°40.110’
Cpx-Am-Bt-Fs/Fd-(Ap-Ttn)
o
CRE-3 N 49°43.726’ E 18°18.349’
Cpx-Am-Fs/Fd-(Ap-Ttn)
x
CT-1
N 49°34.257’ E 18°13.442’
Cpx-Am-Bt-Fs/Fd-(Ap-Ttn)
xxx
CJ-1
N 49°31.813’ E 17°58.190’
Cpx-Am-Bt-Fs/Fd-(Ap-Ttn)
xx
CBL-1 N 49°34.256’ E 18°00.791’
Cpx-Am-Bt-Fs/Fd-(Ap)
x
CR-1
N 49°47.70’ E 18°38.37’
Cpx-Am-Fs/Fd-(Ap)
o
CRE-2 N 49°43.572’ E 18°18.700’
Cpx-Am-Bt-Fs/Fd-(Ap)
x
CR-8
N 49°47.70’ E 18°38.45’
Cpx-Am-Fs/Fd-(Ap- Ttn)
xx
CHB-1 N 49°44.900’ E 18°25.947’
Cpx-Am-Fs/Fd-(Ap)
xx
CP-3
N 49°43.230’ E 18°40.110’
Cpx-Am-Bt-Fs/Fd-(Ap-Ttn)
x
CB-2
N 49°45.49’ E 18°37.80’
Cpx-Am-Fs/Fd-(Ap-Ttn)
x
CZ-1
N 49°34.527’ E 18°02.799’
Fs/Fd-Am-Bt-(Ap)
xxxx
Syenites
CB-4
N 49°46.11’ E 18°37.00’
Cpx-Fs-(Ap)
xxxx
CB-5
N 49°46.11’ E 18°37.00’
Cpx-Fs-(Ap)
xxxx
CZI-1
N 49°44.063’ E 18°26.879’
Fs/Fd-Cpx-(Ap-Ttn)
xxx
Minor or accessory minerals are indicated in parentheses. The degree of secondary alterations:
ο — fresh rock, x — small, xx — medium, xxx — strong, xxxx — very strong. Teschenite CP-1* was
exceptionally highly altered with no primary rock-forming minerals preserved, and thus it was used only
for titanite dating. Abbreviations: Cpx — clinopyroxene, Am — amphibole, Bt — dark mica,
Fs — feldspar, Fd — feldspathoid, (Ap) — accessory apatite, (Ttn) — accessory titanite.
Table 1: GPS coordinates, modal composition and the intensity of secondary alterations
of the Teschenite Association Rock samples.
U–Pb dating
Laser ablation
RESOlution M-50
Wavelength
193 nm (ArF)
Pulse length
20 ns
Fluence at sample
2 J/cm
2
Repetition rate
5 Hz
Spot size
40 µm
Mass spectrometer
ICP MS XseriesII
RF power (W)
1400
Sample gas Ar flow (L/min)
c. 0.8
Cool gas Ar flow (L/min)
13
Auxiliary gas Ar flow (L/min)
c. 0.9
Nitrogen flow (mL/min)
5-6
He flow (L/min)
c. 0.3
Background measurements (s)
40
Ablation time (s)
40
Washout time (s)
35
Scanned masses
43
Ca,
206
Pb,
207
Pb,
208
Pb,
232
Th,
238
U
Dwell time (ms)
5, 50, 50, 30, 30, 20
Table 2: Instrument parameters and analytical conditions of laser-
ablation ICP-MS analyses.
226
BRUNARSKA and ANCZKIEWICZ
GEOLOGICA CARPATHICA
, 2019, 70, 3, 222–240
Table 3: Major (wt. %) and trace element (ppm) concentrations of the Teschenite Association Rocks.
Rock type:
Picrite
Teschenite
Sample no.:
CPR-1
CM-1
CSTa-2
CBS-1
CS-4
CR-6
CP-4
CRE-3
CT-1
CJ-1
CBL-1
CR-1
CRE-2
SiO
2
39.8
37.79
42.16
42.22
40.97
42.38
43.24
45.58
37.74
38.89
40.6
41.33
41.52
TiO
2
0.96
1.92
2.32
2.77
2.09
3.15
3.02
2.69
3.83
2.91
3.15
2.79
3.03
Al
2
O
3
4.45
6.21
9.72
12.36
11.66
11.97
12.94
16.67
11.26
14.19
15.15
17.7
14.27
Fe
2
O
3T
12.71
12.27
8.47
9.86
11.51
10.51
10.61
9.89
14.57
10.86
12.76
11.57
10.68
MnO
0.2
0.2
0.14
0.15
0.16
0.15
0.14
0.17
0.25
0.19
0.2
0.18
0.13
MgO
28.33
17.87
13.83
7.8
8.97
8.49
7.16
3.99
6.41
5.73
5.45
4.66
7.01
CaO
4.5
12.45
15.65
14.32
14.21
16.44
14.94
7.77
11.89
12.6
12.47
10.06
11.7
Na
2
O
0.54
0.4
1.14
1.53
2.88
1.68
2.04
5.21
1.99
3.44
3.29
2.32
1.77
K
2
O
0.64
1.42
1.14
2.74
1.06
1.19
2
2.55
2.38
1.61
1.93
3.27
2.45
P
2
O
5
0.18
1.42
0.37
0.71
1.02
0.45
0.55
0.96
1.76
1.07
0.75
0.8
0.67
LOI
6.8
7.1
4.3
5.1
4.9
3.2
2.8
4.1
7.3
7.9
3.6
4.8
6.30
Total
99.11
99.05
99.24
99.56
99.43
99.61
99.44
99.58
99.38
99.39
99.35
99.48
99.53
Mg#
72.1
71.5
66.8
68.5
70.6
69.3
69.5
68.6
74.4
69.8
72.1
70.7
69.5
TOT/C
0.11
0.17
0.36
0.51
0.4
0.03
<0.02
0.02
1.08
1.14
0.02
0.05
0.40
TOT/S
0.08
0.09
0.07
0.48
0.16
<0.02
0.12
0.04
0.41
0.21
<0.02
0.06
0.12
LILE
Cs
0.5
1.1
0.5
1.7
3.6
1.9
5.3
3.5
1.8
3.2
0.3
2.7
1.8
Rb
18.5
25.9
37
53.7
25.7
22.5
57.5
45.8
60
39.3
34.7
66.2
61.5
Ba
246
1138
1025
1046
805
412
995
1106
1009
1195
1023
1211
994
Sr
248.2
912.7
726.7
730.3
1293.6
621.3
1389.9
1028.8
1411.3
1737.2
2251.4
1814.5
1070.3
HFSE
Th
1.9
11.9
5
6.5
10.2
5
6
10
9.5
15.5
7.2
9.3
9.2
U
0.6
3.6
1.6
1.9
3
1.1
1.6
3.3
2.9
4.5
1.7
1.6
2.9
Nb
25.6
118.5
47.3
77.1
80.4
54
64.6
116.7
117.5
134.5
102.2
106.5
91.5
Ta
1.3
5.5
2.8
4.6
4.4
3.2
4
6.7
7.2
7.3
5.9
6.5
5.5
Pb
1.5
6.2
2.1
3
3.9
3.1
2.4
5.2
4.8
5.7
3
3
3.80
Zr
62.6
337.2
154.7
198.9
192.5
196.6
197
272.1
494.6
380.8
208.5
212.4
242.4
Hf
1.6
6.8
4.5
4.9
4.1
5.5
5.3
5.6
12.4
7.2
4.5
4.1
5.4
Y
8.6
28.5
17.6
24.3
31.7
21.9
23.2
31.4
44.1
31.9
26.7
23.5
28.0
REE
La
18.5
99.7
37.7
56.3
87.5
41
47.9
77.4
103.4
107
67.8
67
61.7
Ce
31
181.3
68.8
108.8
157.5
78.8
86.4
146
209.7
193.7
122.3
119.5
115.6
Pr
3.48
19.86
7.82
12.54
16.68
9.21
10.19
15.85
25.48
19.89
13.11
12.64
12.92
Nd
14
75.4
31.2
51.6
61.7
37.4
42.2
60.4
102.1
74
51.4
46.2
48.7
Sm
2.49
13.19
6.23
10.04
10.95
7.81
8.6
10.82
19.36
13.03
9.38
8.39
9.38
Eu
0.76
3.85
2.00
3.11
3.55
2.39
2.84
3.49
5.91
4.07
2.93
2.76
3.03
Gd
2.42
10.95
5.68
8.66
9.44
7.1
8.04
9.69
15.91
10.71
8.01
7.45
8.52
Tb
0.34
1.35
0.8
1.16
1.33
0.96
1.09
1.43
2.12
1.42
1.14
1.01
1.21
Dy
1.79
6.29
4.25
6.15
6.64
4.99
5.48
7.12
10.91
7.15
6.34
5.27
6.09
Ho
0.32
1.04
0.75
1.06
1.23
0.9
0.97
1.31
1.87
1.23
1.13
0.93
1.09
Er
0.75
2.56
1.74
2.4
3.05
2.12
2.41
3.18
4.4
3.13
2.81
2.49
2.70
Tm
0.11
0.32
0.24
0.32
0.41
0.27
0.32
0.42
0.58
0.41
0.37
0.37
0.35
Yb
0.61
1.77
1.3
1.76
2.32
1.65
1.9
2.43
3.21
2.32
2.22
1.98
2.15
Lu
0.09
0.23
0.19
0.25
0.32
0.22
0.24
0.36
0.44
0.31
0.31
0.27
0.30
Transition metals
Cr
855.3
431.1
845.0
78.7
143.7
23.9
47.9
<0.002
<0.002
<0.002
<0.002
<0.002
<0.002
Co
105.2
63.7
37.6
36.3
42.4
37
36.4
24.3
37.2
33.5
42.6
36.8
37.8
Ni
709.3
638.2
90.7
20.8
108.7
21.6
20
1.3
27
26.2
17.9
11.2
26.6
Sc
14
15
57
23
22
47
30
4
16
9
11
6
16
V
131
164
225
246
207
305
276
167
226
270
336
289
286
Cu
17.2
144
42.7
58.8
59.7
71.2
58.5
15.6
93.6
69.7
57.2
52.7
73.80
Zn
69
119
34
78
79
55
40
72
147
106
51
45
72.00
Ga
6.9
11.6
13.5
15.6
15.5
16.4
17.8
20.3
21.6
20.6
18.7
18.9
18.4
Sn
<1
3
1
2
2
3
2
2
4
1
1
1
2
W
2.2
1.6
<0.5
<0.5
2.7
2
0.5
3.8
1.9
1.3
2.1
0.7
3.2
Mo
1.4
0.5
2.3
2.1
4.3
0.2
1.3
1.8
1.8
3.8
0.7
0.9
2.3
227
TESCHENITES FROM THE TYPE-LOCALITY IN THE OUTER WESTERN CARPATHIANS
GEOLOGICA CARPATHICA
, 2019, 70, 3, 222–240
Petrography and mineral
chemistry
The Teschenite Association Rocks
show wide range of compositional and
textural variations (Table 3 and Fig. 2)
on a regional, as well as on a single
intrusion scale (see also Smulikowski
1929, 1980; Mahmood 1973; Kudě lás-
ková 1987; Hovorka & Spišiak 1988;
Narębski 1990; Dostal & Owen 1998;
Harangi et al. 2003; Włodyka 2010;
Matýsek et al. 2018). Well-preserved
samples, generally, are panidiomorphic,
fine- to coarse-grained and have por-
phyritic, microporphyritic or ophitic
tex
tures. Phenocrysts are clinopyro-
xene, amphibole, olivine, biotite,
phlogopite and feldspar. Matrix has
composition similar to the phenocrysts
but may also contain altered glass and
secondary analcime. Apatite and Fe–Ti
oxides occur as minor or accessory
mine rals. Below we present petrogra-
phy of the main rock types that were
subjected to the detailed geochemical,
isotopic and geochronological studies.
Due to high degree of alterations, pre-
cise classification is often problematic,
and thus, we applied simplified subdivi-
sion distinguishing three main lithologi-
cal types: 1) ultramafic picrite, 2) the most
common, mesocratic teschenite, and
rich in felsic minerals 3) mesocratic
sye nite. Electron microprobe analyses
of the selected phenocrysts are presen-
ted in Supplementary Table S1.
Picrites (CPR-1, CM-1) are relatively
rare and typically poorly preserved.
Fairly fresh picrite represented by sam-
ple CPR-1 consists mainly of olivine,
Ca-amphibole (Ti-rich pargasite and
Ti-rich ferro-pargasite), clinopyroxene
(diopside), phlogopite, spinel, apatite
and opaque minerals (Table S1).
Olivine (Fo
82
–Fo
85
) has CaO content
> 0.3 wt. % which rules out the direct
mantle origin (Simkin & Smith 1970;
Sato et al. 1991). Poikilitic amphibole,
with no signs of recrystallization or
alteration, surrounds smaller crystals of
olivine and diopside (Fig. 2a). This indi-
cates that the sample is a cumulate and
amphibole probably represents inter-
cumulus liquid of nephelinitic compo-
sition consolidated around cumulus
Rock type:
Teschenite
Syenite
Sample no.:
CR-8
CHB-1
CP-3/11
CB-2
CZ-1
CB-4
CB-5
CZI-1
SiO
2
41.74
41.92
43.29
46.83
41.56
47.63
47.04
48.92
TiO
2
2.67
2.66
2.91
2.21
3.5
2.29
2.28
3.13
Al
2
O
3
17.07
15.68
13.01
17.1
14.27
15.03
15.13
13.91
Fe
2
O
3T
11.05
11.8
11.44
7.69
11.21
10.28
9.84
12.76
MnO
0.19
0.2
0.17
0.13
0.16
0.13
0.13
0.16
MgO
4.12
4.78
6.75
4.47
4.55
5.45
5.09
4.22
CaO
10.7
10.03
14.17
8.17
7.31
6.97
7.89
6.40
Na
2
O
2.81
4.31
2.09
4.42
4.63
4.4
4.46
4.65
K
2
O
2.47
2.32
1.93
2.77
1.05
1.57
1.64
1.59
P
2
O
5
0.97
1.19
0.67
0.07
1.04
0.39
0.38
0.45
LOI
5.70
4.60
3.10
5.70
10.20CZ
5.50
5.80
3.05
Total
99.49
99.49
99.53
99.56
99.48
99.64
99.68
99.69
Mg-no.
70.0
70.9
70.5
65.8
70.2
68.5
69.0
72.1
TOT/C
0.04
0.02
0.04
0.07
1.73
0.28
0.5
0.15
TOT/S
<0.02
0.10
0.15
0.06
0.16
0.04
0.12
<0.02
LILE
Cs
3.9
0.8
2.9
9.6
4.2
2.8
3.5
0.8
Rb
50
47.5
45.5
49.9
23.2
25.2
25.9
27.3
Ba
1120
1197
829
1325
735
748
845
644
Sr
1650.7
1077.1
597
545.5
1321.5
1003.5
951.9
727.4
HFSE
Th
8.6
11.8
7.0
10.4
9.0
3.0
2.9
4.4
U
1.8
3.8
1.6
2.9
1.7
0.1
0.9
1.5
Nb
103.1
108.9
84.5
129.7
113.6
37.9
36.9
51.3
Ta
6.7
6.1
5.0
8.6
7.0
2.2
2.4
3.2
Pb
3.20
4.40
3.00
13.9
2.50
2.40
1.90
2.30
Zr
209.5
223.5
204.5
260.7
396.4
130.8
126.4
191.1
Hf
4.2
4.4
5.0
5.1
8.6
3.4
3.3
4.6
Y
26.0
29.6
25.4
20.3
33.5
19.0
18.3
26.0
REE
La
74.1
93.1
58.7
53.7
82.1
26.1
25.4
43.0
Ce
134.5
158.0
106.5
92.1
162.5
48.3
47.2
77.5
Pr
14.25
16.81
11.94
9.87
18.56
5.87
5.63
8.78
Nd
53.6
62.3
47.5
34.7
73.1
24.7
24.0
35.2
Sm
9.45
10.93
8.96
6.08
13.49
5.33
5.25
7.32
Eu
2.98
3.48
3.00
2.03
4.22
1.92
1.86
2.39
Gd
8.08
9.33
7.99
5.52
11.44
5.32
5.18
7.24
Tb
1.14
1.27
1.11
0.82
1.60
0.80
0.77
1.07
Dy
5.90
6.80
5.83
4.58
8.43
4.18
4.07
5.40
Ho
0.97
1.15
1.00
0.85
1.44
0.79
0.81
0.99
Er
2.41
2.87
2.48
2.14
3.49
1.97
1.96
2.51
Tm
0.34
0.39
0.35
0.30
0.45
0.26
0.24
0.32
Yb
2.02
2.40
1.90
1.87
2.42
1.41
1.39
2.01
Lu
0.29
0.32
0.27
0.24
0.33
0.19
0.19
0.27
Transition metals
Cr
<0.002
<0.002
88.9
27.4
<0.002
13.7
13.7
<0.002
Co
34.6
38.9
38.3
22.6
24.4
32.1
32.6
34.5
Ni
7.3
9.4
21.4
13.2
11.1
40.3
43.8
22.4
Sc
5
5
26
25
7
16
15
16
V
274
261
268
175
215
175
173
254
Cu
38.9
39.3
66.6
28.5
55.1
63.6
64.3
133.1
Zn
63
66
63
95
107
83
81
111
Ga
18.7
19.7
18.1
16.7
21.9
16.5
16.2
18.0
Sn
2
2
2
2
2
2
1
2
W
1.5
1.5
3.2
0.8
1.9
1.3
2.0
1.9
Mo
0.4
1.6
0.4
0.8
3.2
0.4
0.8
0.6
Table 3 (continued): Major (wt. %) and trace element (ppm) concentrations of the Teschenite
Association Rocks.
228
BRUNARSKA and ANCZKIEWICZ
GEOLOGICA CARPATHICA
, 2019, 70, 3, 222–240
composed of olivine, spinel, and clinopyroxene (Best 1970;
Dawson 1982). Secondary alterations are expressed as chlori-
tization of phlogopite and serpentinization of olivine. Locally,
rare carbonate crystals were observed. Unlike CPR-1, picrite
CM-1 is severely altered. It comprises relics of clinopyroxene
with numerous olivine inclusions pseudomorphosed by ser-
pentine, phlogopite, apatite and opaque minerals.
The studied teschenites are fine- to coarse-grained, typically
with porphyritic textures. Phenocrysts are formed by clinopy-
roxene, amphibole and dark mica set in fine crystalline matrix
500 µm
500 µm
500 µm
500 µm
500 µm
Ap
Ap
Ttn
Cpx
Cpx
Fs
Fs
Fs
Am
Chl
Am
Cpx
Chl
Chl
Cpx
Chl
Ap
Chl
Chl
Am
500 µm
Srp
Ol
Am
Ol
a
b
c
d
f
e
Ap
Fig. 2. Photomicrographs of the TAR samples: a — olivine enclosed in a large amphibole in picrite CPR-1 (XPL); b — elongated apatite and
titanite in fine-grained matrix, teschenite CT-1 (PPL); c — sector zoning and partial chloritization of clinopyroxene in teschenite CRE-2 (XPL);
d — clinopyroxene and amphibole surrounded by feldspars, in syenite CZI-1 (XPL); e — partly chloritized amphibole with clinopyroxene
inclusion in teschenite CR-6 (XPL); f — chlorite pseudomorph after pyroxene in syenite CB-4 (PPL). Abbreviations: Am — amphibole;
Chl — chlorite; Cpx — clinopyroxene; Ol — olivine; Srp — serpentine; Fs — feldspar; Ttn — titanite; Ap — apatite. XPL — cross polarized
light; PPL — plane-polarized light. See text for details.
229
TESCHENITES FROM THE TYPE-LOCALITY IN THE OUTER WESTERN CARPATHIANS
GEOLOGICA CARPATHICA
, 2019, 70, 3, 222–240
composed of the same minerals with an addition of alkali feld-
spars, and the secondary analcime. Apatite and opaques occur
as minor or accessory minerals. Idiomorphic apatite crystals
are common inclusions in the phenocrysts and in matrix
(Fig. 2b). In some samples accessory amount of titanite is
present (Fig. 2b). Clinopyroxene of diopside composition,
locally with hedenbergite rims (Table S1), forms idiomorphic
crystals often exhibiting sector zoning (Fig. 2c). In some sam-
ples, it occurs as radial aggregates with younger generation
overgrowing the earlier diopside. Amphibole frequently over-
grows diopside or dark mica and displays wide range of com-
positions. Typically, it shows rimward increase in Fe, Ti, Si
accompanied by decrease in Mg. The core composition corre-
sponds to kaersutite while rim is formed by ferro- pargasite,
hastingsite or ferro-kaersutite (Table S1). Rare dark mica
crystals are of biotite–annite composition (Table S1).
Feldspars are represented chiefly by K-feldspar, albite and
rare K–Na-feldspar. Feldspars are commonly carbonatized.
Partial chloritization of amphibole is also frequently observed
(Fig. 2d).
The most felsic type of the TAR is represented by rare
syenites (CZI-1, CB-4, CB-5) characterized by considerably
lower mafic phenocrysts/matrix ratio. Phenocrysts are repre-
sented by clinopyroxene (diopside, seldom augite) and amphi-
bole (kaersutite, Table S1). Matrix is composed of K-feldspar,
albite and secondary analcime (Fig. 2e). Clinopyroxene and
amphibole crystals are corroded or partly chloritized along
edges and fractures or even entirely chloritized (Fig. 2f).
Chlorite aggregates occur also between feldspar crystals.
Ilmenite, Fe-oxides and titanite form skeletal and needle-
shaped aggregates. Small apatite crystals are abundant as
inclusions in feldspar and in the phenocrysts.
In addition to alterations described above, saussuritization
and zeolitisation are observed. More detailed account on
secon dary processes in the TAR can be found in Dolníček et
al. (2010a, b, 2012).
Major and trace elements
The chemical composition of the studied samples is given in
Table 3. Despite careful sample selection, some degree of
alteration is an inherent feature of the TAR which is reflected
by the secondary alterations described above but also by
the elevated LOI observed in majority of the collected samples
(3–7 wt. % with an exception of CZ-1 where LOI is as high as
10.2 wt. %).
The studied samples are generally poor in silica (41–51 wt. %
volatile–free) and rich in P
2
O
5
and TiO
2
(Fig. 3a, Table 3).
CIPW-normative compositions show that TAR are, only with
a few exceptions (CB-4, CZI-1, CT-1), strongly silica-under-
saturated (normative nepheline up to 15 wt. %). The content of
MgO is 4–28 wt. % and Mg# = (MgO/(MgO + FeO
t
)) × 100 (in
molar proportions) varies from 40 to 82 (Table 3).
According to TAS classification (Le Bas et al. 1986) they
are mainly basanites or tephrites with smaller number of
picrobasalts, basaltic trachyandesites, basalts and one sample
classifies as a phonotephrite (Fig. 3a). Because the degree of
major element mobility linked to the secondary alterations has
not been quantified, which may cast some doubts on accuracy
of this classification, we additionally present classification
based on “immobile” trace elements following Pearce (1996).
In the latter classification the studied and the previously pub-
lished teschenites fall within the alkaline fields of alkali
basalts, trachybasalts, tephrites, basanites and, similarly to
TAS classification, one sample falls within the phonotephrite
field (Fig. 3b). Thus, both classifications are largely consistent
(Fig. 3a and b).
In the Fenner-type variation diagrams of major-element
oxides vs. MgO, two distinct trends are revealed. An inflected
trend is observed for CaO and TiO
2
, while Al
2
O
3
and Na
2
O
show a gently curved, convex-downward trend. The remai-
ning oxides (SiO
2
and P
2
O
5
) do not follow any obvious regular
pattern (Fig. 4).
Picro-
basalt
Basalt
Basaltic
andesite
Trachyte
Phonolite
Tephriphonolite
Phonotephrite
Foidite
Tephrite
Basanite
T
rachy-
basalt
Basaltic
trachy-
andesite
T
rachyandesite
Andesite
0
2
4
6
8
10
14
16
Na
O +
KO
(wt.%
)
22
12
40
50
60
SiO (wt.%)
2
Ultrabasic
Intermediate
Basic
e
n
il
a
k
l
a
e
n
il
a
k
l
a
b
u
s
picrite
teschenite
syenite
published
data
a)
Basalt
Alkali
basalt
Foidite
Ande
site
Basal
tic an
desite
Trach
y-
andesi
te
Tephr
iphon
olite
Rhyolite
Dacite
Trachyte
Phonolite
Alkali
rhyolite
0.01
0.1
1
10
100
0.
001
0.
005
0.
05
0.
5
Nb/Y
Zr/Ti
b)
Fig. 3. a — Total Alkali Silica classification diagram (Le Bas et al. 1986); b — Nb/Y vs. Zr/Ti classification of Pearce (1996) for the studied
TAR (coloured symbols) and the published data shown in grey (Dostal & Owen 1998; Harangi et al. 2003; Włodyka 2010).
230
BRUNARSKA and ANCZKIEWICZ
GEOLOGICA CARPATHICA
, 2019, 70, 3, 222–240
Aug
Di
Di
Aug
Di
Aug
Aug
Di
Aug
Par
Kaer
Par
Kaer
Par
Kaer
Kaer
Di
Kaer
Par
Par
Phl
Bt
Phl
Bt
Phl
Bt
Phl
Bt
Phl
Bt
Ol
Ol
Ol
Ol
Ol
Si
O
[wt%
]
2
0
5
25
10
15
20
30
45
55
30
50
60
35
40
65
Al
O
[wt%
]
2
3
0
5
25
10
15
20
30
8
20
4
16
24
12
CaO [wt%
]
0
5
25
10
15
20
30
10
20
5
15
25
Na
O [wt%
]
2
0
5
25
10
15
20
30
2
6
1
4
7
3
5
a)
b)
c)
d)
e)
f)
MgO [wt%]
PO
[wt%
]
2
5
0
5
25
10
15
20
30
1
3
2
4
MgO [wt%]
Ti
O
[wt%
]
2
0
5
25
10
15
20
30
1
3
2
4
picrite
teschenite
syenite
literature data
avarage
phenocrysts
composition
All samples show mutually comparable abundances of trace
elements, with an exception of picrite CPR-1 that displays sig-
nificantly lower trace-element contents (Fig. 5). However, all
samples display generally strong enrichment in incompatible
over more compatible elements expressed as a negative slope
in primitive-mantle normalized spider diagram (Fig. 5a). A little
smaller degree of enrichment is observed for the syenites
(Fig. 5a). Besides the negative slope, other features common
for our samples are: negative Rb, K, Pb and Hf anomalies,
positive Nb, Ta, Ba, LREE and, less conspicuous, Sr anomaly
(Fig. 6a). Similarly chondrite-normalized REE diagram dis-
plays sub-parallel, linear patterns with high enrichment in
more incompatible light REE (La
n
/Yb
n
= 12–38) and no Eu
anomalies (Fig. 5b). In absolute values, light REE enrichment
is the highest in the picrites and the lowest in the syenites.
Heavy REE show very low normalized values and display
Fig. 4. Fenner diagrams of MgO vs.: a — SiO
2
; b — Al
2
O
3
; c — CaO; d — Na
2
O; e — P
2
O
5
and f — TiO
2
. The previously published data
shown in grey (Dostal & Owen 1998; Harangi et al. 2003; Włodyka 2010). Average chemical composition of the phenocrysts according to
the microprobe analyses presented in Table S1. Abbreviations: Aug — augite; Di — diopside; Ol — olivine; Kaer — kaersutite; Par — par-
gasite; Bt — biotite; Phl — phlogopite.
231
TESCHENITES FROM THE TYPE-LOCALITY IN THE OUTER WESTERN CARPATHIANS
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11
01
00
100
0
Rb
Ba
Th
U
Ta
Nb
K
La
Ce
Pb
Pr
Sr
Nd
Hf
Zr
Sm
Eu
Ti
Dy
Y
Yb
Lu
Sa
mp
le
/P
rimi
tive
Ma
nt
le
teschenite
picrite
syenite
La
Pr
Pm
Eu
Tb
Ho
Tm
L
u
Ce
Nd
Sm
Gd
Dy
Er
Yb
1
10
100
100
0
Sa
mp
le
/R
EE
chondr
ite
average OIB
a)
b)
much less variations in abundance in comparison to that
observed for light REE.
Laser-ablation ICP-MS U–Pb titanite dating
The dating results obtained for six samples are summarized
in the Supplementary Table S2 and Fig. 6. Each sample was
analyzed during an individual session during which the secon-
dary standard measurements were accurate within ≤ 1 % 2 RSD
(2 relative standard deviations) and yielded the weighted mean
age of 520.9 ± 3.5 Ma (MSWD = 2.0, n = 7).
We analyzed 20–40 crystals depending on abundance of
titanite in a sample. Expectedly, the analyses show significant
and variable amounts of common Pb. Crystals virtually com-
mon Pb-free are scarce and were found only in sample CHB-1
from Horní Bludovice (Fig. 6). Nevertheless, the obtained
dating results reveal a rather coherent picture. Intercept ages
with Terra-Wasserburg concordia and
207
Pb-corrected weighted
mean ages show slight variations but are indistinguishable
within the estimated uncertainties.
Five out of six samples gave nearly identical lower intercept
ages between 117.9 ± 1.8 and 119.3 ± 1.4 Ma (MSWD < 2 for
all samples). Only teschenite CT-1 from Tichá yielded an older
age of 123.7 ± 2.1 Ma (Fig. 6) which was confirmed by a repli-
cate measurement. Due to a high closure temperature of
the U–Pb system in titanite (e.g., Villa 1998; Cherniak 2000)
and very fast cooling of small bodies emplaced into a cold
shallow crust, we interpret the obtained ages as reflecting
the time of intrusive TAR emplacement.
Isotope geochemistry
Whole-rock Sr, Nd and Hf isotope compositions are pre-
sented in Table 4. Initial
143
Nd/
144
Nd and
176
Hf/
177
Hf ratios
(corrected for emplacement age t = 120 Ma) yielded a very
narrow range of ε(Nd)
i
= 5.0 to 6.3 and wider range of
ε(Hf)
i
= 4.9 to 10.0 shown in Figure 7a–b. This results in a steep
array in ε(Nd)
i
–ε(Hf)
i
diagram, intersecting the Terrestrial Array
of Vervoort et al. (2011). Unlike Nd and Hf isotopes,
87
Sr/
86
Sr
i
initial ratios vary broadly from 0.7032 to 0.7071 (Fig. 7a).
Discussion
Fractional crystallization
Except for the cumulate picrite CPR-1, the other samples of
the TAR do not fulfil the requirements for mantle primary par-
tial melts, and thus they must have undergone some degree of
differentiation (Green & O’Hara 1971; Gill 2010). The signi-
ficance of fractional crystallization (FC) process is suggested
by the presence of geochemical trends showing higher varia-
tions in compatible relatively to incompatible trace elements
(Fig. 8) and the presence of cumulate texture in picrite CPR-1.
The inflected trend in the MgO–CaO diagram (Fig. 4c) implies
that the magmas were most likely subjected to two stages of
differentiation: (1) CaO increase probably related to olivine
crystallization, and (2) CaO decrease likely related to fractio-
nation of clinopyroxene. The first stage could have led to
the formation of relatively primitive teschenites (e.g. CS-4) and
the second fractionation step would have led to the formation
of the more evolved teschenites and syenites. The negative
correlations of MgO vs. Na
2
O, Al
2
O
3
and SiO
2
, as well as
the absence of Eu anomaly suggest that feldspar fractionation
did not play any significant role in TAR formation (Figs. 4
and 5b).
Crustal contamination
Trace-element ratios sensitive to crustal contamination (e.g.,
Th/La, Zr/Nb, Ba/Nb, La/Nb) along with Nb/Yb vs. Th/Yb
discrimination diagram of Pearce (2008) shown in Fig. 9a
Fig. 5. Spider diagrams: a — primitive-mantle normalized trace-elements, normalization values after McDonough & Sun (1995); b — chon-
drite-normalized REE, normalization values after Boynton (1984). Average ocean island basalt (OIB) composition after Sun & McDonough
(1989).
232
BRUNARSKA and ANCZKIEWICZ
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, 2019, 70, 3, 222–240
argue against the significant crustal involvement in the magma
genesis of the TAR. Similarly, narrow range of positive
ε(Nd)
i
= 5.0–6.3 and ε(Hf)
i
= 4.9–10.0 point to very little, if any,
crustal contamination (see also Dostal & Owen 1998; Harangi
et al. 2003). High and diverse
87
Sr/
86
Sr values (Fig. 7a), which
typically point to the crustal involvement, are most likely
a result of interaction with the Nd-poor and Sr-rich liquids,
possibly sea or diagenetic water (Rossy et al. 1992; Dolníček
et al. 2010b).
Partial melting
High enrichment in incompatible elements, Zr/Nb = 2.0–4.2,
K/Nb < 179, decreasing La/Yb ratios with increasing SiO
2
content along with the positive ε(Nd)
i
and ε(Hf)
i
values, imply
that parental magmas may have formed by the small degree
of partial melting of a mantle source (Fig. 9b). TiO
2
/Yb vs.
Nb/Yb diagram of Pearce (2008) points to a rather deep,
garnet peridotite melting (Fig. 9c). The presence of the resi-
dual garnet in the source is also suggested by the low
HREE content and strong light to heavy REE fractionation
(Fig. 5b).
Using the GCDkit (Janoušek et al. 2006, 2016) and
PETROMODELER software (Ersoy 2013), we conducted
modelling of non-modal batch melting adapting initial mantle
source composition of Clague & Frey (1982) together with
the modified modal garnet and spinel peridotite compositions of
Bradshaw et al. (1993). We used the distribution coefficients
0.0
0.1
0.2
0.3
0.4
0.5
0.6
0
10
20
30
40
50
60
238
U/
206
Pb
207
Pb
/
206
Pb
data-point error ellipses are 2σ
Intercept at
119.3 ± 1.4 Ma
MSWD = 1.4
80
100
120
140
160
180
0.0
0.1
0.2
0.3
0.4
0.5
0.6
0
10
20
30
40
50
60
238
U/
206
Pb
207
Pb
/
206
Pb
data-point error ellipses are 2σ
Intercept at
118.5 ± 1.7 Ma
MSWD = 1.6
90
100
110
120
130
140
150
0.0
0.1
0.2
0.3
0.4
0.5
0.6
0
10
20
30
40
50
60
238
U/
206
Pb
207
Pb
/
206
Pb
data-point error ellipses are 2σ
Intercept at
118.7± 1.4 Ma
MSWD = 1.4
85
95
105
115
125
135
145
CZi-1-12, syenite, Žermanice
CR8, teschenite, Rudów
CP11, teschenite Puńców
119.7 ± 1.6 Ma
119.2 ± 1.6 Ma
120.8 ± 1.6 Ma
0.0
0.1
0.2
0.3
0.4
0.5
0.6
0
10
20
30
40
50
60
238
U/
206
Pb
207
Pb
/
206
Pb
data-point error ellipses are 2σ
Intercept at
123.7± 2.1 Ma
MSWD = 1.5
90
100
110
120
130
140
150
160
125.6 ± 2.0 Ma
CT1-12, teschenite Tichá
0.0
0.1
0.2
0.3
0.4
0.5
0.6
0
10
20
30
40
50
60
238
U/
206
Pb
20
7
Pb
/
20
6
Pb
data-point error ellipses are 2σ
Intercept at
117.9 ± 1.8 Ma
MSWD = 1.7
CHB1-12, teschenite, Horní Bludovice
90
100
110
120
130
140
150
160
118.9 ± 1.9 Ma
0.0
0.1
0.2
0.3
0.4
0.5
0.6
0
10
20
30
40
50
60
238
U/
206
Pb
20
7
Pb
/
20
6
Pb
data-point error ellipses are 2σ
Intercept at
118.1 ± 1.6 Ma
MSWD = 1.6
95
105
115
125
135
118.8 ± 2.2 Ma
CR-6, teschenite, Rudów
Fig. 6. Laser-ablation ICP-MS U–Pb titanite dating results. Ellipses represent 2σ errors.
233
TESCHENITES FROM THE TYPE-LOCALITY IN THE OUTER WESTERN CARPATHIANS
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, 2019, 70, 3, 222–240
Sample
Lithology
Sm [ppm]
Nd [ppm]
147
Sm/
144
Nd
143
Nd/
144
Nd
εNd
(120)
T
DM
Nd
(Ga)
Rb
[ppm]
Sr
[ppm]
87
Rb/
86
Sr*
87
Sr/
86
Sr
87
Sr/
86
Sr
(120)
Lu
[ppm]
Hf
[ppm]
176
Lu/
177
Hf
176
Hf/
177
Hf
εHf
(120)
CPR-1
picrite
2.65
13.1
1
0.1221
0.512879±4
5.9
0.30
18.5
248.2
0.2051
0.703562±16
0.703218
0.09
1.63
0.0082
0.282985±5
9.1
CM-1
picrite
14.02
79.20
0.1071
0.512834±7
5.2
0.32
25.9
912.7
0.0781
0.704200±10
0.704069
0.24
7.16
0.0048
0.282858±5
4.9
CST
a-2
teschenite
6.45
30.68
0.1271
0.512864±9
5.5
0.34
37.0
726.7
0.1401
0.704025±13
0.703790
0.19
4.43
0.0062
0.282944±6
7.8
CBS-1
teschenite
10.17
48.03
0.1280
0.512862±10
5.4
0.35
53.7
730.3
0.2024
0.703719±1
1
0.703379
0.23
4.92
0.0067
0.282933±5
7.4
CS-4
teschenite
11.31
62.79
0.1089
0.512877±10
6.0
0.27
25.7
1293.6
0.0547
0.703700±10
0.703608
0.34
4.25
0.01
12
0.282998±5
9.3
CR-6
teschenite
8.04
38.92
0.1250
0.512869±6
5.6
0.33
22.5
621.3
0.1
139
0.703737±1
1
0.704949
0.23
5.84
0.0056
0.282973±4
8.9
CP-4
teschenite
9.21
41.74
0.1334
0.512882±9
5.8
0.34
57.5
1390
0.1225
0.705140±12
0.703775
0.24
5.38
0.0064
0.282963±5
8.4
CRE-3
teschenite
11.54
61.72
0.1
131
0.512850±9
5.4
0.32
45.8
1029
0.0997
0.703981±1
1
0.703570
0.34
5.84
0.0083
0.282961±5
8.2
CT
-1
teschenite
18.50
94.80
0.1
180
0.512834±8
5.0
0.36
60.0
141
1
0.1
170
0.703856±12
0.703660
0.41
12.34
0.0048
0.282930±6
7.4
CJ-1
teschenite
12.95
73.1
1
0.1071
0.512830±8
5.1
0.33
39.3
1737
0.0424
0.704137±8
0.706056
0.32
7.29
0.0061
0.282943±5
7.8
CBL-1
teschenite
9.20
49.01
0.1
134
0.512863±7
5.7
0.30
34.7
2251
0.1582
0.706127±12
0.704500
0.31
4.63
0.0095
0.283007±6
9.8
CRE-2
teschenite
9.46
48.94
0.1
169
0.512847±9
5.3
0.33
61.5
1070
0.0623
0.704765±9
0.704033
0.29
5.49
0.0074
0.282950±6
7.9
CR-8
teschenite
10.09
56.06
0.1088
0.512856±8
5.6
0.30
50.0
1651
0.1214
0.704536±9
0.704031
0.29
4.29
0.0095
0.282984±7
9.0
CHB-1
teschenite
10.62
60.19
0.1067
0.512848±9
5.5
0.30
47.5
1077
0.0833
0.704235±12
0.704396
0.32
4.35
0.0103
0.282970±5
8.4
CP-3
teschenite
9.14
46.28
0.1
194
0.512870±8
5.7
0.31
45.5
597.0
0.2098
0.705755±1
1
0.705403
0.27
5.13
0.0076
0.282980±6
9.0
CZ-1
teschenite
13.22
68.85
0.1
161
0.512858±8
5.6
0.32
23.2
1322
0.0483
0.703980±1
1
0.703899
0.32
8.84
0.0051
0.282949±5
8.1
CB-4
syenite
5.58
24.42
0.1383
0.51291
1±16
6.2
0.30
25.2
1004
0.0691
0.707240±10
0.707124
0.21
3.51
0.0083
0.282999±4
9.6
CB-5
syenite
5.47
23.90
0.1383
0.512909±8
6.2
0.31
25.9
951.9
0.0749
0.706193±1
1
0.706067
0.20
3.39
0.0085
0.28301
1±10
10.0
CZI-1
syenite
7.69
70.07
0.0663
0.512858±8
6.3
0.21
27.3
727.4
0.1033
0.704629±8
0.704456
0.28
5.00
0.0078
0.283000±6
9.7
All
errors
are
2SE
(standard
errors)
and
relate
to
the
last
significant
digits.
Concentrations
determined
by
isotope
dilution
method,
except
for
Rb
and
Sr
which
were
determined
by
ICP-MS.
Uncertainty
of
87
Rb/
86
Sr
,
147
Sm/
144
Nd and
176
Lu/
177
Hf
ratios are 1 %, 0.3 % and 0.5 %, respectively
. Normalizing ratios, decay constants, model values used for the calculations along with standards reproducibility are given in the main text.
from Kostopoulos & James (1991). Details of
model ling parameters are presented in Table 5.
The calculated melting curves plotted in the Zr/Nb
vs. Ce/Y plot (Fig. 10a) show that nearly all samples
presented in this study, and the vast majority of
the published data, could have originated by 2–5 %
partial melting of peridotite containing ca. 2.5 to
6.0 % of garnet (Fig. 10a). Only very few samples
reported by Włodyka (2010) show better fit with
a curve portraying the partial melting of a spinel-
bearing source. Additionally, we calculated melting
curves in the Yb
n
–Ce
n
/Yb
n
space which is more
sensitive to the presence of garnet and spinel in
the source (Fig. 10b). This projection clearly exclu-
des the possibility of melting in the spinel stability
field suggested in Fig. 10a and by Harangi et al.
(2003). Furthermore, it narrows down the range of
garnet content in the source to ca. 4–6 %. At the same
time, it suggests slightly wider range of melting
fractions from 2.5 to 10 %. However, in this respect,
inferences based on Fig. 10a seem more adequate, as
Zr/Nb ratio is more sensitive to the degree of partial
melting. The subhorizontal shift of some data in
the direction of higher Yb
n
content seems to be asso-
ciated with magma differentiation or very the low
abundance of garnet, but not with the presence of
spinel in the source.
Our modelling results show that the low degree of
partial melting of the metasomatized garnet perido-
tite, with, or without, fractional crystallization, could
well explain the trace-element variations in practi-
cally all the TAR.
Magma source
Geochemical signature of the TAR places them in
the group of alkaline within-plate basalts with dis-
tinct OIB affinity as inferred on the basis of the pro-
jections shown in Figure 9a and c of Pearce (2008).
This is additionally supported by the relative enrich-
ment in the incompatible trace elements (Fig. 5) and,
typical of OIB, HFSE ratios such as Zr/Y = 7–13,
Zr/Nb = 2–4 and Nb/Yb = 18–76 (Ulrych et al. 1993).
The negative anomalies of Rb, K and Pb with the high
primitive-mantle normalized Nb and Ta contents
(Fig. 5a) further constrain magma source as a HIMU-
type OIB (Wilson & Downes 1991). The enrichment
in LILE relative to HFSE indicates the presence of
an enriched component together with HIMU and
the depleted mantle signature (Fig. 11).
Although the HIMU reservoir was initially
defined on the basis of the highly radiogenic Pb iso-
tope composition, it is also characterized by the dis-
tinct Nd–Hf isotope systematics (Woodhead 1996;
Hanyu et al. 2012; Nebel et al. 2013). The HIMU
acquired fractionated (Sm–Nd)/(Lu–Hf) relative to
Table 4:
Summary of Rb–Sr
, Sm–Nd and Lu–Hf isotope analyses of the
Teschenite
Association Rocks. Initial
87
Sr/
86
Sr
i
ratios, ε(Nd)
i
and ε(Hf)
i
calculated for emplacement time t = 120 Ma.
234
BRUNARSKA and ANCZKIEWICZ
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, 2019, 70, 3, 222–240
the BSE, and thus the HIMU-derived magmatic rocks plot sig-
nificantly below the Terrestrial Array, forming its own, much
steeper linear trend (Fig. 7b). Only sample CM-1 displays
the same systematics as typical HIMU rocks from St. Helena
and Mangaia (Cook–Austral Islands). The remaining samples
lie within, or on the prolongation of the field defined mostly
by more radiogenic Cook–Austral samples (Fig. 7b). The most
radiogenic TAR fall into the OIB field, close to the Terrestrial
Array. Thus, we interpret the observed Nd–Hf isotopic sys-
tematics as a result of mixing between components derived
from HIMU-type and less fertile component like MORB type
basalts (Fig. 7b).
As mentioned above, Sr isotopes are of little use when it
comes to constraining petrogenesis of the TAR. However, it is
noteworthy that the lowest
87
Sr/
86
Sr
i
coupled with a very nar-
row range of ε(Nd)
i
values seem to converge near the HIMU
field which well agrees with the general picture derived from
the Nd–Hf isotopes (Fig. 7a).
Although high concentration of the incompatible elements
could be primarily due to the low degree of partial melting,
the significant degree of mantle metasomatism is indicated by
the abundance of amphibole, apatite or phlogopite even in
the most primitive samples. The depletion of K and Rb relative
to Ba, Nb and Ta (Fig. 5a) points to the presence of the residual
amphibole and/or phlogopite in the mantle source. The domi-
nant role of amphibole is inferred on the basis of high K/Rb
(>250) and low Rb/Sr (<0.09) in the melts (Furman & Graham
1999; Ulrych et al. 2011), and on the basis of the common
occurrence of this phase in the European mantle xenoliths
(Downes 2001). Volatile-rich mantle domains could have ori-
ginated due to infiltration of subduction-related fluids from
the recycled oceanic crust possibly during the Variscan
Fig. 7. Sr–Nd–Hf isotope composition of the TAR: a — initial
87
Sr/
86
Sr
i
vs. ε(Nd)
i
and b — initial ε(Nd)
i
vs. ε(Hf)
i
diagrams. Initial ratios
corrected fort the emplacement time t = 120 Ma. Terrestrial Array after Vervoort et al. (2011). Published Sr–Nd isotope data for the Pyrenees
from Rossy et al. (1992), for the Carpathians from Dostal & Owen (1998), Harangi et al. (2003), for Central and Western Europe from Wilson
& Downes (2006); Nd–Hf isotope data for Vogelsberg area from Jung et al. (2011), for Rhӧn area from Jung et al. (2005) and Jung & Hoernes
(2000), HIMU, OIB, EM, DM data from Woodhead (1996), Chauvel et al. (1997), Salters and White (1998), Hanyu et al. (2012), Nebel et al.
(2013). Lower part of the field is shown for the most extreme HIMU signature from St. Helena and Mangaia (Cook–Austral Islands).
10
20
50
100
200
500
1000
1
5
10
50
100
500
1000
Zr [ppm]
Ni [ppm
]
Ni [ppm
]
0.5
1
5
10
50
500
0.5
Yb [ppm]
a)
b)
picrite
teschenite
syenite
FC
PM
1
5
10
50
100
500
Fig. 8. Log–log diagrams showing relationship between incompatible (Zr, Yb) and compatible (Ni) elements in response to dominantly partial
melting (PM) or fractional crystallization (FC) processes, indicated by tentatively estimated vectors: a — Zr vs. Ni and b — Yb vs. Ni.
235
TESCHENITES FROM THE TYPE-LOCALITY IN THE OUTER WESTERN CARPATHIANS
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, 2019, 70, 3, 222–240
Orogeny. As also pointed out by Dostal & Owen (1998), this is
suggested by the depleted mantle Nd model ages (0.26–0.36 Ga:
Table 4). The presence of the recycled oceanic crust at the depth
of 400–600 km in the Central European mantle was proposed
on the basis of seismic tomography studies (Piromallo et al.
2001).
The presence of the HIMU asthenospheric mantle in Europe
is often explained in the context of hot fingers derived from
a mantle plume (Wilson & Bianchini 1999). So called “super
plume event”, involving mantle upwellings worldwide, started
at ca. 120 Ma (Larson 1991), i.e. during the TAR emplace-
ment. Harangi et al. (2003) proposed that Cape Verde plume
activity, that triggered central Atlantic opening, could either
have channelled the HIMU component in the N–NE direction
or pollute the upper mantle layer beneath Europe, leading to
the formation of the common European Asthenospheric
Reservoir (EAR, Cebriá & Wilson 1995). Mantle plume may
have generated mafic, volatile-rich intrusions that caused
the upper mantle metasomatism (Bogaard & Wӧrner 2003;
Seghedi et al. 2004a).
An alternative scenario requires transport of the deep mantle
material with the HIMU signature to the volatile-rich upper
mantle, in response to adiabatic decompression and passive
upwelling. Adiabatic decompression rather than mantle plume
is our preferred mechanism given the short duration and small
volume of TAR volcanism as well as an overall extensional,
incipient rift setting in the studied region during Early
Cretaceous. Since the volatile-rich mantle domains melt more
readily, even small decompression would induce melting.
Adiabatic decompression appears to have played a significant
role also in generating Cenozoic magmatism in Europe
(Wilson & Downes 2006; Lustrino & Wilson 2007).
Timing of TAR emplacement
There have been several attempts of dating alkaline rocks
from the OWC. Lucińska-Anczkiewicz et al. (2002) conducted
Ar–Ar dating of kaersutites and obtained a tight group of ages
for the three mesocratic teschenites, yielding a weighted mean
age of 122.3 ± 3.2 Ma. Dating of an additional syenite sample
by the same authors gave a little younger, but still overlapping
within the analytical precision, age of 120.4 ± 2.6 Ma. This led
the authors to a suggestion that the more evolved magma
could have intruded slightly later.
These coherent results, suggesting short duration of alkaline
magmatism in the area, are in marked contrast to the subse-
quent geochronological studies. The reported K–Ar ages of
amphibole, biotite and whole-rock fractions vary widely from
63.6 ± 1.6 to 148.6 ± 3.6 Ma (Grabowski et al. 2003) and from
96.3 ± 3.7 to 128.3 ± 5.6 Ma (Harangi et al. 2003). Grabowski
et al. (2003) explained the wide range of ages as a result of
hydrothermal alterations but the oldest, biotite ages spanning
from 137.9 ± 2.0 to 133.1± 1.8 Ma were interpreted as reliable
and reflecting the time of biotite crystallization during
teschenites emplacement. Szopa et al. (2014) applied in situ
LA ICP-MS U–Pb apatite dating that resulted in two rather
imprecise ages of 103 ± 20 and 127 ± 9 Ma. The third sample
from Puńców gave fairly precise 119.6 ± 3.2 Ma age, confir-
ming earlier Ar–Ar dating results of Lucińska-Anczkiewicz et
al. (2002) from the same locality (120.4 ± 2.6 Ma). The recent
Fig. 9. Incompatible element ratios diagrams: a — Nb/Yb vs. Th/Yb
(Pearce 2008); b — SiO
2
vs. La/Yb; c — Nb/Yb vs. TiO
2
/Yb (Pearce
2008). Data from the previous studies shown in grey (Dostal & Owen
1998; Harangi et al. 2003; Włodyka 2010).
236
BRUNARSKA and ANCZKIEWICZ
GEOLOGICA CARPATHICA
, 2019, 70, 3, 222–240
U–Pb dating of apatite from the Žermanice sill, using laser
ablation multi collector ICP-MS, also provides an imprecise
120 ± 10 Ma age, interpreted as the time of sill emplacement
(Matýsek et al. 2018).
High scatter among the published K–Ar ages is almost cer-
tainly caused by the well acknowledged excess Ar problems,
in the studied area caused, at least partly, by very strong alte-
rations in the vast majority of the TAR. High common Pb in
apatite, on the other hand, along with the low U content, are
responsible for the low precision of in situ U–Pb dating, which
makes such ages of limited use. Taking into account the pub-
lished interpretations of the previous geochronological stu dies,
teschenites in the Outer Western Carpathians would have been
emplaced between 138 and 105 Ma with the most repro ducible
ages grouping around 105 to 123 Ma. This suggests ca. 20
to even 30 Ma long period of alkaline magmatism during
the Early Cretaceous. Our new U–Pb titanite dating of five
teschenites and one syenite are in good agreement with
the Ar–Ar data of Lucińska-Anczkiewicz et al. (2002). Five
out of six samples gave unresolvable within the analytical pre-
cision ages between 117.9 ± 1.8 and 119.3 ± 1.4 Ma (Fig. 6).
Notably, severe alterations in the teschenite CP-1 from
Puńców did not have any negative consequences for our dating
results. The U–Pb system in titanite must have remained intact
as indicated by a very good age consistency with the four other
samples. Only teschenite CT-1 from Tichá area gave an older
123.7 ± 2.1 Ma age that we interpret as reflecting the earlier
emplacement time.
On the whole, our results along with the ages of Lucińska-
Anczkiewicz et al. (2002) indicate that small portions of partial
melts were extruded, or emplaced into a shallow crust, within
a rather short period of time, between 124 and 119 Ma.
Geodynamic implications
The Early Cretaceous to Neogene mafic alkaline rocks from
Western and Central Europe show similar geochemical and
isotopic systematics (Rossy et al. 1992; Hovorka & Spišiak
1993; Hovorka et al. 1999; Ivan et al. 1999; Harangi 2001;
Spišiak & Balogh 2002; Harangi et al. 2003; Seghedi et al.
2004a, b; Wilson & Downes 2006; Jung et al. 2011; Spišiak et
al. 2011; Oszczypko et al. 2012) Wide areal extent of geo-
chemically and isotopically similar igneous activity implies
the presence of a relatively long-lived, enriched reservoir in
the upper mantle which likely can be correlated with European
Asthenospheric Reservoir (EAR) as defined by Cebriá &
10%
8%
6%
4%
2%
2.5% Gr
t
6% Gr
t
10%
8%
6%
4%
2%
5% Sp
10%
6%
4%
2%
1%
mantle source
composition
picrite
teschenite
syenite
1
2
3
4
5
6
7
8
1
2
3
4
5
6
7
8
9
10
0
0
Ce/Y
Zr/Nb
10
15
20
25
30
35
5
10
15
20
25
30
35
40
0
0
(Ce/Yb)n
(Yb)n
literature data
6% Gr
t
4% Gr
t
5% Sp
10%
8%
2%
2%
4%
4%
5%
6%
10%
10%
6%
8%
4%
8%
3%
3%
1%
a)
b)
5
FC
Fig. 10. Trace-elements based petrogenetic partial melting model of the TAR magmas calculated using GCDkit (Janoušek et al. 2006) and
PETROMODELLER software (Ersoy 2013). Data from the previous studies shown in grey (Dostal & Owen 1998; Harangi et al. 2003;
Włodyka 2010). Modelling parameters summarized in Table 5.
Mantle source modal composition and melting modes, modified from
Bradshaw et al. (1993)
%
Ol
Opx
Cpx
Grt
Sp
Proportion of phases
Spinel periditite
60
20
15
0
5
Garnet peridotite 2.5 %
60
23
14.5
2.5
0
Garnet peridotite 4 %
60
22.5
13.5
3
0
Garnet peridotite 6 %
60
22.5
11.5
6
0
Contribution to melt
Spinel periditite
10
10
50
0
30
Garnet peridotite 2.5 %
10
30
55
5
0
Garnet peridotite 4 %
10
30
55
5
0
Garnet peridotite 6 %
10
30
55
5
0
Trace element composition of mantle source (Clague & Frey 1982)
ppm
Zr
Nb
Ce
Y
Yb
20
4
5.44
6
0.6
Partition coefficients (Kostopulous & James 1992)
Zr
Nb
Ce
Y
Yb
Ol
0.1
0.0001
0.000008
0.01
0.0194
Opx
0.03
0.001
0.00105
0.1
0.0631
Cpx
0.16
0.015
0.0389
0.2
0.19
Spl
0.05
0.0001
0.000008
0.0078
0.00032
Grt
0.32
0.04
0.0014
2.2885
4.7
Table 5: Input parameters used for of non-modal batch melting
modelling shown in Fig. 10. Abbreviations: Ol — olivine, Opx —
orthopyroxene, Grt — garnet, Sp — spinel.
237
TESCHENITES FROM THE TYPE-LOCALITY IN THE OUTER WESTERN CARPATHIANS
GEOLOGICA CARPATHICA
, 2019, 70, 3, 222–240
Wilson (1995). Our study of the TAR shows that their petro-
genesis, indeed, can be associated with EAR, as also suggested
by Harangi et al. (2003). The Cretaceous mafic alkaline volca-
nism, including volumetrically minor alkaline magmatism in
the Outer Western Carpathians, is interpreted as a result of
the incipient rift zone formation that triggered opening of
the Alpine Tethys and the North Pyrenean Rift Zone.
The Teschenite Association Rocks occur exclusively within
the Silesian Nappe which constitutes central part of the former
Outer Western Carpathians Basin. This basin formed as
a result of rifting within the southern passive margin of
the European Plate, possibly due to the eastward escape and
rotation of the Alcapa and Tisia blocks in the Late Jurassic to
Early Cretaceous (Słomka 1986; Ślączka et al. 1999; Spišiak
et al. 2011). Rift never evolved to a sea-floor spreading stage
(Nemčok et al. 2001) and the maximum extent of the Outer
Western Carpathians Basin was reached during Hauterivian–
Aptian (Książkiewicz 1960). Maximum lithospheric thinning
achieved during Early Aptian possibly triggered the adiabatic
decompression and the partial melting in the volatile-rich
metasomatized asthenospheric mantle. Our dating results indi-
cate that the extension climax was accompanied by short
(~ 5 Myr) episode of alkaline magmatism lasting from ca. 124
to 119 Ma. The short duration of the magmatic activity in
the Silesian Basin could be related to a major stress
reorganization in the region. The maximum extension that we
correlate with the TAR emplacement was followed in the south-
eastern Outer Carpathians by the compressive regime in
the Aptian–Albian (Sandulescu 1988; Kruglov 1989). This
compressional phase was also manifested by uplift of the intra-
basin ridges, the siliciclastic turbidites deposition and the syn-
sedimentary folding in the Silesian and Magura basins
(Švábenická et al. 1997; Oszczypko 2006). Hence, it seems
plausible to assume that rapid transition from the extensional
climax to the compressive regime during the Aptian could
have ceased mafic alkaline magmatism in the Silesian Basin.
Conclusions
The Jurassic–Early Cretaceous formation of the rift-related
sedimentary basins in the northern part of the Tethys Ocean
was accompanied by alkaline magmatism. A suite of the ultra-
basic to intermediate Teschenite Association Rocks was
emplaced within the Silesian Basin due to small degree of par-
tial melting of the metasomatized asthenospheric mantle likely
accompanied by some degree of the two-stage fractional crys-
tallization. Melting was triggered by the maximum litho-
spheric thinning associated with rifting and adiabatic
decompression at the southern margin of the European Plate.
Rb/Nb
Ba/N
b
b)
a)
c)
d)
La/Th
Rb/Th
U/Pb
Rb/La
HIMU
EMI
EMII
EMI
EMII
HIMU
EMII
EMI HIMU
EMII
EMI
HIMU
Ce/Pb
Ba/L
a
picrite
teschenite
syenite
0.5
1.0
1.5
2.0
2.5
01
02
03
04
0
0.2
0.3
0.4
0.5
0.6
0.7
0.8
0.9
01
02
03
04
05
06
07
0
0
5
10
15
20
05
10
152
0
0.5
1.0
1.5
05
10
15
20
25
Fig. 11. Trace-element ratios diagrams: a — Rb/Nb vs. Ba/Nb; b — Rb/Th vs. La/Th; c — U/Pb vs. Ce/Pb and d — Rb/La vs. Ba/La showing
fields characteristic of ocean-island basalts derived from HIMU, EMI and EMII mantle end-members (Willbold & Stracke 2006).
238
BRUNARSKA and ANCZKIEWICZ
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, 2019, 70, 3, 222–240
About 2–5 % of partial melting occurred most likely within
the volatile-rich mantle domains in the garnet stability field.
Mantle metasomatism might have been induced by the earlier,
Variscan subduction events. The Nd–Hf isotopic signature,
together with the incompatible trace-elements composition,
indicate the HIMU-type OIB mantle source mixed with the more
“depleted”, probably MORB-type component. The geochemi-
cal and isotopic characteristics point to the genesis associated
with the European Asthenospheric Reservoir — the common
mantle end-member for the widespread Cenozoic volcanic
rocks in Europe — that seems important also for the Cretaceous
mafic volcanism in Central and Western Europe.
In situ U–Pb titanite dating indicates that the TAR were
emplaced over a short period of time between 124 and 119 Ma
(Aptian) during maximum lithospheric thinning in the Outer
Western Carpathians Basin. Magmatic activity ceased during
the major stress reorganization associated with the transition
to the dominantly compressive regime between the southern
European margin and North Africa.
Acknowledgments: This project was funded by Polish Natio-
nal Science Centre grant no. 2011/01/B/ST10/04683. We thank
Zdeněk Dolníček for his help in the field and creative discus-
sions and Jakub Bazarnik as well as Dariusz Sala for their
laboratory and field assistance. We are grateful to Skår Øyvind
and Allen Kennedy for sharing titanite standards. We are
indebted to Vojtěch Janouśek and an anonymous reviewer for
providing very detailed and helpful reviews. We are grateful to
Milan Kohút and Igor Petrík for the editorial handling of
the manuscript.
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i
TESCHENITES FROM THE TYPE-LOCALITY IN THE OUTER WESTERN CARPATHIANS
GEOLOGICA CARPATHICA
, 2019, 70, 3, 222–240
Supplement
Table S1: Electron microprobe analyses of the selected phenocrysts.
Representative pyroxene compositions from Teschenite Association Rocks samples
Rock type:
Picrite
Picroteschenite
Mineral:
Di
Di
Di
Di
Di
Di
Di
Di
Di
Di
Di
Di
Sample:
CPR1-1
CPR1-1
CS4-2.
CS4-2.
CS4-3
CS4-3
CSTa2-2
CSTa2-2
CR6-2
CR6-2
CR6-4
CR6-4
2
8
2
3
4
5
8
11
5
9
4
5
uniform
uniform bright rim dark core bright zone dark zone dark core very bright
rim
dark zone bright zone bright core dark zone
SiO
2
46.79
47.86
43.59
50.37
47.96
49.86
47.17
48.87
48.52
43.70
43.31
46.59
TiO
2
2.18
2.13
3.39
1.25
1.94
1.46
2.61
1.34
2.08
3.25
3.97
2.70
Al
2
O
3
6.62
5.97
8.63
3.36
5.20
3.68
5.73
2.28
4.48
7.86
8.30
6.21
Cr
2
O
3
0.76
0.77
0.01
0.39
0.04
0.21
0.47
0.07
0.01
0.00
0.00
0.12
Fe
2
O
3
4.06
3.27
5.62
3.26
4.60
3.29
3.89
4.34
2.95
5.67
5.67
4.15
FeO
1.80
1.93
2.76
2.31
2.85
2.66
1.96
11.20
3.65
3.28
2.33
1.94
MnO
0.04
0.08
0.11
0.08
0.14
0.11
0.00
0.53
0.17
0.09
0.04
0.00
MgO
13.38
13.88
11.13
15.02
13.53
14.67
13.80
8.05
13.63
11.07
11.52
13.27
CaO
24.10
24.17
23.66
23.93
23.71
23.90
23.97
22.43
23.78
23.55
23.97
24.21
Na
2
O
0.29
0.30
0.45
0.33
0.34
0.30
0.32
1.04
0.28
0.41
0.37
0.33
K
2
O
0.00
0.01
0.02
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.01
0.00
Total
100.02
100.38
99.37
100.30
100.32
100.14
99.92
100.14
99.56
98.88
99.49
99.52
No. oxyg.
6
6
6
6
6
6
6
6
6
6
6
6
Si
1.737
1.765
1.648
1.854
1.780
1.841
1.752
1.884
1.812
1.664
1.636
1.739
Ti
0.061
0.059
0.096
0.035
0.054
0.041
0.073
0.039
0.058
0.093
0.113
0.076
Al
0.290
0.260
0.385
0.146
0.227
0.160
0.251
0.104
0.197
0.353
0.369
0.273
Cr
0.022
0.022
0.000
0.011
0.001
0.006
0.014
0.002
0.000
0.000
0.000
0.004
Fe3+
0.113
0.091
0.160
0.090
0.129
0.091
0.109
0.126
0.083
0.162
0.161
0.117
Fe2+
0.056
0.060
0.087
0.071
0.088
0.082
0.061
0.361
0.114
0.104
0.073
0.060
Mn
0.001
0.002
0.004
0.002
0.004
0.003
0.000
0.017
0.005
0.003
0.001
0.000
Mg
0.740
0.763
0.627
0.824
0.748
0.808
0.764
0.463
0.759
0.629
0.649
0.739
Ca
0.959
0.955
0.959
0.944
0.943
0.946
0.954
0.927
0.951
0.961
0.970
0.968
Na
0.021
0.021
0.033
0.024
0.024
0.021
0.023
0.078
0.020
0.030
0.027
0.024
K
0.000
0.000
0.001
0.000
0.000
0.000
0.000
0.000
0.000
0.000
0.000
0.000
Total
4.000
4.000
4.000
4.000
4.000
4.000
4.000
4.000
4.000
4.000
4.000
4.000
Mg no.
0.930
0.928
0.878
0.921
0.894
0.908
0.926
0.562
0.869
0.857
0.898
0.924
All analyses by electron microprobe; Di - diopside, He - hedenbergite, Aug - augite
ii
BRUNARSKA and ANCZKIEWICZ
GEOLOGICA CARPATHICA
, 2019, 70, 3, 222–240
Representative pyroxene compositions from Teschenite Association Rocks samples
Rock type:
Teschenite
Syenite
Mineral:
Di
Di
Di
Di
He
Di
Di
He
Di
Di
He
Di
Di
Aug
Aug
Sample:
CBL1-2 CBL1-2 CRE3-1 CRE3-1 CRE3-2 CRE3-3 CRE3-3 CRE3-3 CRE3-4 CRE3-4 CRE3-4 CZI1-1 CZI1-1 CZI1-1 CZI1-4
21
22
12
19
32
33
7
8
7
11
12
9
10
13
1
uniform uniform dark zone bright
zone
bright
rim
dark core brighter
zone
very
bright rim dark core
brighter
zone 2
very
bright rin uniform uniform uniform uniform
SiO
2
44.46
41.97
49.36
44.57
46.15
46.14
47.56
46.31
48.93
49.9
46.7
49.45
48.64
51.23
50.44
TiO
2
3.31
4.57
1.85
3.54
1.82
2.62
2.12
1.46
1.96
1.39
1.74
1.81
2.13
0.85
0.99
Al
2
O
3
7.86
9.44
4.06
6.99
2.75
5.71
4.79
2.11
3.85
3.09
3.01
3.46
4.08
1.95
2.39
Cr
2
O
3
0.00
0.03
0.00
0.01
0.00
0.01
0
0
0.01
0.01
0
0
0.01
0
0
Fe
2
O
3
5.27
5.80
3.42
5.08
6.33
4.22
3.31
4.68
3.38
2.13
4.49
2.78
3.28
1.37
2.54
FeO
2.50
2.94
3.62
3.79
17.74
6.92
6.34
19.77
3.88
7.14
15.33
5.97
5.92
9.82
7.83
MnO
0.10
0.08
0.17
0.09
0.94
0.33
0.27
0.99
0.11
0.26
0.86
0.17
0.2
0.36
0.37
MgO
11.88
10.61
13.72
11.50
2.22
9.94
11
1.68
13.67
11.95
4.53
13.67
13.45
13.76
14.22
CaO
23.86
23.70
23.47
23.04
19.72
22.95
23.08
19.94
23.28
23.26
20.84
22.03
21.81
20.05
20.35
Na
2
O
0.38
0.43
0.51
0.55
1.92
0.68
0.63
1.57
0.45
0.52
1.38
0.43
0.44
0.35
0.34
K
2
O
0.01
0.00
0.00
0.01
0.00
0
0.02
0.03
0
0
0.01
0.01
0
0
0
Total
99.63
99.57
100.18
99.17
99.59
99.52
99.12
98.54
99.52
99.65
98.89
99.78
99.96
99.74
99.47
No. oxyg.
6
6
6
6
6
6
6
6
6
6
6
6
6
6
6
Si
1.672
1.591
1.830
1.691
1.859
1.761
1.808
1.895
1.829
1.881
1.863
1.850
1.820
1.926
1.896
Ti
0.094
0.130
0.052
0.101
0.055
0.075
0.061
0.045
0.055
0.039
0.052
0.051
0.060
0.024
0.028
Al
0.348
0.422
0.177
0.312
0.131
0.257
0.215
0.102
0.170
0.137
0.142
0.153
0.180
0.086
0.106
Cr
0.000
0.001
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
Fe3+
0.149
0.165
0.095
0.145
0.192
0.121
0.095
0.144
0.095
0.060
0.135
0.078
0.092
0.039
0.072
Fe2+
0.079
0.093
0.112
0.120
0.598
0.221
0.202
0.677
0.121
0.225
0.512
0.187
0.185
0.309
0.246
Mn
0.003
0.003
0.005
0.003
0.032
0.011
0.009
0.034
0.003
0.008
0.029
0.005
0.006
0.011
0.012
Mg
0.666
0.600
0.758
0.650
0.133
0.565
0.624
0.102
0.762
0.671
0.269
0.762
0.750
0.771
0.797
Ca
0.961
0.963
0.932
0.936
0.851
0.938
0.940
0.874
0.932
0.939
0.891
0.883
0.874
0.808
0.819
Na
0.028
0.032
0.037
0.040
0.150
0.050
0.046
0.125
0.033
0.038
0.107
0.031
0.032
0.026
0.025
K
0.000
0.000
0.000
0.000
0.000
0.000
0.001
0.002
0.000
0.000
0.001
0.000
0.000
0.000
0.000
Total
4.000
4.000
4.000
4.000
4.000
4.000
4.000
4.000
4.000
4.000
4.000
4.000
4.000
4.000
4.000
Mg no.
0.894
0.865
0.871
0.844
0.182
0.719
0.756
0.132
0.863
0.749
0.345
0.803
0.802
0.714
0.764
All analyses by electron microprobe; Di - diopside, He - hedenbergite, Aug - augite
Table S1 (continued): Electron microprobe analyses of the selected phenocrysts.
iii
TESCHENITES FROM THE TYPE-LOCALITY IN THE OUTER WESTERN CARPATHIANS
GEOLOGICA CARPATHICA
, 2019, 70, 3, 222–240
Representative amphibole compositions from Teschenite Association Rocks samples
Group:
OH,F,Cl
OH,F,Cl
oxo
oxo
OH,F,Cl
OH,F,Cl
OH,F,Cl
OH,F,Cl
OH,F,Cl
oxo
Subgroup:
Ca
Ca
B = Ca
B = Ca
Ca
Ca
Ca
Ca
Ca
B = Ca
Species:
Ti-par
Ti-rich par
ferri-kaer ferro-ferri-kaer Ti-ferro-Par
Ti-par
Ti-Par
Ti-par
K-hast
ferro-ferri-kaer
Sample:
CPR-1-3
CPR-1-3
CRE3-1
CRE3-3
CS4-1
CS4-.
CSTa2-1
CSTa2-1
CBL1-2
CBL1-2
15
16
6
1
1
7
12
21
3
4
uniform
uniform
uniform
overgrowth on
px
uniform
rim on px
uniform
uniform
bright rim
dark core
SiO
2
40.49
41.07
39.08
39.13
37.73
37.51
40.10
39.15
35.21
35.25
TiO
2
3.86
3.63
5.08
4.65
2.91
3.55
4.20
4.20
0.64
4.38
ZrO
2
0.02
0.02
0.04
0.05
0.13
0.06
0.06
0.00
0.03
0.08
Al
2
O
3
13.95
13.37
12.39
11.91
14.30
15.66
13.17
13.75
14.58
15.95
Cr
2
O
3
0.22
0.12
0.00
0.01
0.00
0.00
0.05
0.04
0.02
0.01
MnO
0.10
0.10
0.33
0.47
0.45
0.34
0.18
0.21
0.70
0.41
Mn
2
O
3
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
FeO
8.22
8.24
10.66
13.34
17.35
15.13
12.03
12.24
25.89
13.16
Fe
2
O
3
0.00
0.00
7.39
6.51
1.65
0.89
0.00
0.08
5.04
8.08
NiO
0.06
0.08
0.07
0.00
0.02
0.02
0.00
0.09
0.00
0.02
MgO
14.33
14.61
8.62
7.25
7.79
9.15
12.11
12.00
0.24
5.22
CaO
12.43
12.42
11.82
11.46
11.59
12.01
12.12
12.19
10.52
11.89
Na
2
O
2.66
2.53
2.66
2.68
2.26
2.33
2.60
2.53
1.86
1.92
K
2
O
1.39
1.43
1.11
1.29
1.53
1.46
1.37
1.38
2.66
1.84
H
2
O
+
2.05
2.02
0.76
0.84
1.90
1.96
1.96
2.01
1.81
0.81
F
0.00
0.06
0.12
0.10
0.11
0.03
0.11
0.00
0.06
0.24
Cl
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
O=F,Cl (calc)
0.00
-0.03
-0.05
-0.04
-0.05
-0.01
-0.05
0.00
-0.03
-0.10
Total
99.78
99.67
100.08
99.65
99.68
100.09
100.01
99.87
99.22
99.16
No. oxyg.
22
22
22
22
22
22
22
22
22
22
Si
5.936
6.021
5.979
6.069
5.815
5.685
5.967
5.853
5.773
5.548
Al
2.064
1.979
2.021
1.931
2.185
2.315
2.033
2.147
2.227
2.452
Ti
0.000
0.000
0.000
0.000
0.000
0.000
0.000
0.000
0.000
0.000
Fe3+
0.000
0.000
0.000
0.000
0.000
0.000
0.000
0.000
0.000
0.000
[T]
8.000
8.000
8.000
8.000
8.000
8.000
8.000
8.000
8.000
8.000
Ti
0.426
0.400
0.585
0.543
0.337
0.405
0.470
0.472
0.079
0.519
Zr
0.001
0.001
0.003
0.004
0.010
0.004
0.004
0.000
0.002
0.006
Al
0.346
0.331
0.214
0.246
0.413
0.482
0.277
0.276
0.591
0.507
Cr
0.026
0.014
0.000
0.001
0.000
0.000
0.006
0.005
0.003
0.001
Mn
3+
0.000
0.000
0.000
0.000
0.000
0.000
0.000
0.000
0.000
0.000
Fe
3+
0.000
0.000
0.851
0.759
0.193
0.102
0.000
0.009
0.623
0.957
Ni
0.007
0.009
0.009
0.000
0.002
0.002
0.000
0.011
0.000
0.003
Mn
2+
0.012
0.012
0.009
0.039
0.019
0.020
0.023
0.022
0.095
0.051
Fe
2+
1.008
1.010
1.363
1.731
2.236
1.917
1.497
1.531
3.548
1.732
Mg
3.132
3.193
1.966
1.676
1.790
2.067
2.686
2.675
0.059
1.225
[C]
4.958
4.970
5.000
4.999
5.000
4.999
4.963
5.001
5.000
5.001
Mn
2+
0.000
0.000
0.034
0.023
0.040
0.023
0.000
0.005
0.002
0.004
Fe
2+
0.000
0.000
0.000
0.000
0.000
0.000
0.000
0.000
0.000
0.000
Mg
0.000
0.000
0.000
0.000
0.000
0.000
0.000
0.000
0.000
0.000
Ca
1.953
1.951
1.938
1.904
1.914
1.950
1.932
1.953
1.848
1.996
Na
0.047
0.049
0.029
0.073
0.046
0.027
0.068
0.042
0.150
0.000
[B]
2.000
2.000
2.001
2.000
2.000
2.000
2.000
2.000
2.000
2.000
Ca
0.000
0.000
0.000
0.000
0.000
0.000
0.000
0.000
0.000
0.000
Na
0.709
0.670
0.761
0.733
0.629
0.658
0.682
0.691
0.441
0.586
K
0.260
0.267
0.217
0.255
0.301
0.282
0.260
0.263
0.556
0.369
[A]
0.969
0.937
0.978
0.988
0.930
0.940
0.942
0.954
0.997
0.964
OH
2.000
1.972
0.774
0.867
1.946
1.986
1.948
2.000
1.969
0.844
F
0.000
0.028
0.058
0.049
0.054
0.014
0.052
0.000
0.031
0.119
Cl
0.000
0.000
0.000
0.000
0.000
0.000
0.000
0.000
0.000
0.000
O
0.000
0.000
1.168
1.084
0.000
0.000
0.000
0.000
0.000
1.036
[W]
2.000
2.000
2.000
2.000
2.000
2.000
2.000
2.000
2.000
1.999
Total
15.927
15.907
15.979
15.987
15.930
15.939
15.905
15.955
15.997
15.965
All analyses by electron microprobe; Amphibole formula calculated after Locock (2014); Ti-par – Ti-pargasite; Ti-rich par – Ti rich pargasite; ferri-Kaer – ferri kaersutite;
K-hast – K-hastingsite; ferro-ferri-kaer – ferro-ferri-kaersutite
Table S1 (continued): Electron microprobe analyses of the selected phenocrysts.
iv
BRUNARSKA and ANCZKIEWICZ
GEOLOGICA CARPATHICA
, 2019, 70, 3, 222–240
Representative mica compositions from Teschenite Association Rocks samples
Rock:
Picrite
Picroteschenite
Mineral:
Bt
Bt
Bt
Phl
Phl
Phl
Bt
Bt
Bt
Bt
Bt
Bt
Bt
Bt
Sample:
CPR1-1 CPR1-1 CPR1-1 CPR-1-4. CPR-1-4. CPR-1-4. CSTa-2-3 CSTa-2-3 CSTa-2-3 CSTa-2-3 CSTa-2-3 CSTa-2-3 CSTa-2-3 CSTa-2-3
1
2
13
4
6
7
2
3
4
5
6
7
8
9
SiO
2
37.24
36.87
36.56
37.39
36.54
39.35
36.21
37.05
35.88
37.20
36.72
36.86
36.86
37.00
TiO
2
6.07
6.18
5.01
3.61
5.38
3.92
6.02
6.15
6.55
6.14
6.02
5.63
5.96
5.80
Al
2
O
3
17.23
17.19
16.68
16.16
16.97
12.45
16.69
16.80
16.39
16.97
16.56
16.66
16.83
16.86
FeO
7.67
7.42
9.34
7.77
7.80
8.75
11.03
10.21
10.19
10.02
11.15
12.93
11.69
11.88
MnO
0.12
0.12
0.04
0.07
0.07
0.07
0.12
0.07
0.07
0.12
0.10
0.20
0.06
0.09
MgO
18.16
18.29
17.79
19.75
18.60
23.68
15.72
16.57
15.50
16.83
16.02
15.17
15.94
15.97
CaO
0.00
0.00
0.10
0.25
0.15
0.13
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
Na
2
O
0.86
0.86
1.59
1.59
1.06
0.62
0.69
0.73
0.69
0.72
0.70
0.66
0.76
0.67
K
2
O
8.44
8.17
7.32
7.50
8.09
4.90
8.27
8.33
8.18
8.23
8.37
8.55
8.19
8.43
BaO
0.65
0.77
0.39
0.24
0.80
0.50
0.47
0.57
0.76
0.69
0.56
0.50
0.52
0.43
F
0.00
0.09
0.21
0.00
0.11
0.00
0.18
0.03
0.25
0.07
0.13
0.00
0.11
0.02
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
Cr
2
O
3
0.11
0.14
0.11
0.05
0.04
0.00
0.01
0.03
0.00
0.00
0.00
0.00
0.05
0.00
H
2
O
*
4.20
4.14
4.02
4.13
4.10
4.18
3.99
4.14
3.92
4.14
4.06
4.13
4.09
4.15
O=F,Cl
0.00
0.04
0.09
0.00
0.05
0.00
0.08
0.01
0.11
0.03
0.05
0.00
0.05
0.01
Total
100.75
100.20
99.07
98.51
99.66
98.55
99.32
100.67
98.27
101.10
100.34
101.29
101.01
101.29
No. oxyg.
22
22
22
22
22
22
22
22
22
22
22
22
22
22
Si
5.311
5.284
5.323
5.429
5.282
5.645
5.315
5.340
5.317
5.334
5.339
5.352
5.326
5.336
Al iv
2.689
2.716
2.677
2.571
2.718
2.105
2.685
2.660
2.683
2.666
2.661
2.648
2.674
2.664
[T]
8.000
8.000
8.000
8.000
8.000
7.751
8.000
8.000
8.000
8.000
8.000
8.000
8.000
8.000
Al vi
0.207
0.188
0.185
0.194
0.173
0.000
0.202
0.195
0.180
0.202
0.178
0.203
0.193
0.202
Ti
0.651
0.666
0.549
0.394
0.585
0.423
0.665
0.667
0.730
0.662
0.658
0.615
0.648
0.629
Cr
0.012
0.016
0.013
0.006
0.005
0.000
0.001
0.003
0.000
0.000
0.000
0.000
0.006
0.000
Fe
0.915
0.889
1.137
0.943
0.943
1.050
1.354
1.231
1.263
1.202
1.356
1.570
1.413
1.433
Mn
0.014
0.015
0.005
0.009
0.009
0.009
0.015
0.009
0.009
0.015
0.012
0.025
0.007
0.011
Mg
3.861
3.907
3.861
4.275
4.008
5.064
3.440
3.560
3.424
3.597
3.472
3.283
3.433
3.433
[M]
5.661
5.681
5.749
5.821
5.722
6.546
5.677
5.664
5.605
5.678
5.676
5.695
5.699
5.708
Ca
0.000
0.000
0.016
0.039
0.023
0.020
0.000
0.000
0.000
0.000
0.000
0.000
0.000
0.000
Na
0.238
0.239
0.449
0.448
0.297
0.172
0.196
0.204
0.198
0.200
0.197
0.186
0.213
0.187
K
1.535
1.493
1.359
1.389
1.492
0.897
1.548
1.531
1.546
1.505
1.552
1.583
1.509
1.551
Ba
0.036
0.043
0.022
0.014
0.045
0.028
0.027
0.032
0.044
0.039
0.032
0.028
0.029
0.024
[A]
1.809
1.776
1.846
1.889
1.857
1.117
1.772
1.768
1.789
1.744
1.782
1.798
1.752
1.762
Total
15.470
15.456
15.595
15.710
15.580
15.414
15.449
15.432
15.394
15.422
15.458
15.493
15.451
15.471
OH*
4.000
3.959
3.903
4.000
3.950
4.000
3.916
3.986
3.883
3.968
3.940
4.000
3.950
3.991
F
0.000
0.041
0.097
0.000
0.050
0.000
0.084
0.014
0.117
0.032
0.060
0.000
0.050
0.009
Cl
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
Al total
2.896
2.904
2.862
2.766
2.891
2.105
2.888
2.854
2.863
2.868
2.838
2.851
2.866
2.866
Fe/Fe+Mg
0.192
0.185
0.228
0.181
0.190
0.172
0.282
0.257
0.269
0.250
0.281
0.323
0.292
0.294
All analyses by electron microprobe; H
2
O calculations after Tindle & Webb (1990); Bt - biotite, Phl - phlogopite
Table S1 (continued): Electron microprobe analyses of the selected phenocrysts.
v
TESCHENITES FROM THE TYPE-LOCALITY IN THE OUTER WESTERN CARPATHIANS
GEOLOGICA CARPATHICA
, 2019, 70, 3, 222–240
Representative olivine compositions from Teschenite Association Rocks samples
Rock type:
Picrite
Mineral:
Ol
Ol
Ol
Ol
Ol
Ol
Ol
Ol
Formula
CPR1-2
CPR1-2
CPR1-3
CPR1-3
CPR1-3
CPR1-3
CPR1-4
CPR1-4
5
6
9
10
11
12
1
2
MgO
44.13
44.25
44.09
44.65
44.05
42.95
44.62
44.91
CaO
0.48
0.46
0.44
0.33
0.41
0.48
0.42
0.41
MnO
0.30
0.25
0.24
0.25
0.29
0.32
0.32
0.19
FeO(tot)
15.61
15.21
14.63
13.95
14.75
16.59
14.55
14.37
NiO
0.07
0.19
0.16
0.16
0.09
0.15
0.11
0.19
Al2O3
0.03
0.04
0.03
0.04
0.03
0.01
0.02
0.03
Cr2O3
0.01
0.02
0.01
0.02
0.03
0.01
0.02
0.03
SiO
2
40.10
40.30
40.00
40.62
39.98
39.92
40.37
40.67
TiO
2
0.03
0.02
0.02
0.01
0.01
0.02
0.01
0.01
Total
100.77
100.75
99.62
100.04
99.64
100.44
100.45
100.81
No. oxygens
4
4
4
4
4
4
4
4
Mg
1.645
1.646
1.655
1.661
1.654
1.614
1.660
1.662
Ca
0.013
0.012
0.012
0.009
0.011
0.013
0.011
0.011
Mn
0.006
0.005
0.005
0.005
0.006
0.007
0.007
0.004
Fe
2+
(tot)
0.326
0.317
0.308
0.291
0.311
0.350
0.304
0.298
Ni
0.001
0.004
0.003
0.003
0.002
0.003
0.002
0.004
Al
0.001
0.001
0.001
0.001
0.001
0.000
0.001
0.001
Cr
0.000
0.000
0.000
0.000
0.001
0.000
0.000
0.001
Si
1.003
1.006
1.007
1.014
1.007
1.006
1.007
1.009
Ti
0.000
0.000
0.000
0.000
0.000
0.000
0.000
0.000
Total cations
2.996
2.993
2.992
2.985
2.992
2.993
2.992
2.990
Fo%
83.210
83.640
84.100
84.870
83.920
81.890
84.220
84.620
Mg/Mg+Fe
0.835
0.839
0.843
0.851
0.842
0.822
0.845
0.848
Ol - olivine
Table S1 (continued): Electron microprobe analyses of the selected phenocrysts.
vi
BRUNARSKA and ANCZKIEWICZ
GEOLOGICA CARPATHICA
, 2019, 70, 3, 222–240
Table S2: Summary of laser ablation ICP-MS U–Pb titanite dating results.
Isotope ratios
Ages (Ma)
207
Pb/
235
U
±2SE
206
Pb/
238
U ±2SE
238
U/
206
Pb ±2SE
207
Pb/
206
Pb ±2SE
206
Pb/
238
U age
±2SE
207
Pb/
235
U age
±2SE
207
Pb-corr. Age ±2SE
Sample CP1-11
0.520
0.065
0.0219
0.0013
45.66
2.71
0.170
0.023
139.7
8.4
405
44
117.5
9.3
1.050
0.180
0.0255
0.0022
39.22
3.38
0.331
0.063
162.0
14.0
686
90
114.0
21.0
1.000
0.120
0.0256
0.0017
39.06
2.59
0.309
0.040
163.0
11.0
661
61
114.0
12.0
0.548
0.076
0.0215
0.0014
46.51
3.03
0.190
0.029
136.8
9.1
410
49
114.0
11.0
1.161
0.088
0.0271
0.0012
36.90
1.63
0.315
0.025
172.0
7.4
759
40
115.7
9.6
0.431
0.057
0.0210
0.0010
47.53
2.26
0.153
0.021
134.1
6.3
354
41
117.8
8.3
0.356
0.046
0.0217
0.0011
46.08
2.34
0.126
0.017
138.0
7.2
298
34
125.6
8.0
0.432
0.081
0.0229
0.0021
43.67
4.00
0.141
0.031
146.0
14.0
347
59
129.0
14.0
0.430
0.110
0.0205
0.0018
48.78
4.28
0.146
0.037
131.0
11.0
330
78
114.0
14.0
0.447
0.072
0.0225
0.0015
44.44
2.96
0.160
0.028
143.4
9.3
346
50
128.0
12.0
0.484
0.079
0.0217
0.0014
46.08
2.97
0.186
0.036
139.3
9.3
365
51
120.0
12.0
0.759
0.090
0.0238
0.0014
42.02
2.47
0.256
0.033
151.4
8.9
546
52
116.0
11.0
0.416
0.052
0.0217
0.0010
46.15
2.13
0.143
0.020
138.1
6.3
334
38
123.5
8.0
0.405
0.060
0.0203
0.0013
49.26
3.15
0.148
0.023
129.5
8.2
321
42
113.9
9.2
0.439
0.070
0.0204
0.0013
49.02
3.12
0.164
0.028
130.3
8.5
338
48
112.9
9.7
0.396
0.072
0.0224
0.0015
44.64
2.99
0.137
0.027
142.6
9.1
315
52
128.0
11.0
0.476
0.074
0.0217
0.0013
46.08
2.76
0.175
0.032
138.0
8.2
368
51
119.7
9.4
0.570
0.130
0.0223
0.0015
44.84
3.02
0.185
0.038
142.0
9.6
417
73
118.5
9.8
0.308
0.037
0.0201
0.0010
49.70
2.40
0.113
0.015
128.3
6.1
266
29
118.0
6.9
0.372
0.082
0.0218
0.0018
45.87
3.79
0.133
0.031
139.0
12.0
298
60
123.0
12.0
0.400
0.100
0.0219
0.0019
45.66
3.96
0.137
0.035
140.0
12.0
306
71
125.0
13.0
0.506
0.085
0.0216
0.0013
46.30
2.79
0.175
0.029
137.8
8.0
375
54
117.0
9.6
0.429
0.062
0.0211
0.0014
47.39
3.14
0.158
0.026
134.5
9.0
337
44
117.0
11.0
1.310
0.100
0.0289
0.0014
34.60
1.68
0.359
0.038
183.4
9.0
827
45
119.0
13.0
0.511
0.081
0.0223
0.0014
44.84
2.82
0.182
0.031
142.0
8.8
380
53
121.0
10.0
0.373
0.050
0.0214
0.0011
46.73
2.40
0.134
0.019
136.5
7.1
308
38
122.7
8.2
0.640
0.100
0.0234
0.0015
42.74
2.74
0.205
0.035
149.1
9.5
467
63
120.0
13.0
1.280
0.140
0.0290
0.0015
34.48
1.78
0.305
0.033
184.0
9.7
798
59
128.0
12.0
0.446
0.065
0.0227
0.0013
44.05
2.52
0.153
0.025
144.5
8.3
349
43
126.8
9.9
0.422
0.056
0.0223
0.0012
44.84
2.41
0.145
0.021
142.0
7.5
342
41
125.7
9.1
0.985
0.082
0.0259
0.0013
38.61
1.94
0.286
0.025
164.8
7.9
678
44
118.8
9.3
1.590
0.150
0.0301
0.0019
33.22
2.10
0.422
0.050
191.0
12.0
928
61
110.0
15.0
0.630
0.100
0.0233
0.0015
42.92
2.76
0.206
0.030
148.5
9.4
447
58
116.4
9.5
0.351
0.029
0.0204
0.0006
49.02
1.35
0.123
0.010
130.2
3.6
301
21
118.6
4.0
Sample CR8-11
0.530
0.150
0.0231
0.0026
43.29
4.87
0.198
0.060
147.0
17.0
430
110
121.0
20.0
0.330
0.052
0.0224
0.0014
44.64
2.79
0.120
0.022
142.4
8.7
280
41
131.0
9.8
0.416
0.057
0.0210
0.0014
47.62
3.17
0.156
0.023
133.5
9.0
342
43
116.3
9.9
0.334
0.054
0.0203
0.0013
49.26
3.15
0.131
0.024
129.4
8.2
270
40
117.3
9.4
0.328
0.057
0.0217
0.0014
46.08
2.97
0.122
0.022
138.0
8.9
268
42
126.3
10.0
0.316
0.046
0.0197
0.0011
50.76
2.83
0.119
0.019
125.5
6.9
267
36
114.4
7.9
0.482
0.083
0.0221
0.0016
45.25
3.28
0.178
0.035
140.5
10.0
376
57
122.0
13.0
0.368
0.067
0.0209
0.0015
47.85
3.43
0.137
0.025
133.3
9.6
293
49
120.0
11.0
0.350
0.063
0.0191
0.0013
52.36
3.56
0.134
0.024
121.6
8.5
282
47
108.2
9.3
0.397
0.067
0.0202
0.0013
49.50
3.19
0.158
0.030
128.5
8.4
315
49
114.0
10.0
0.368
0.062
0.0195
0.0014
51.28
3.68
0.147
0.026
124.1
9.0
296
45
110.0
10.0
0.285
0.053
0.0210
0.0015
47.62
3.40
0.116
0.025
133.9
9.3
233
39
125.0
11.0
0.358
0.060
0.0206
0.0014
48.54
3.30
0.138
0.026
131.3
8.9
286
43
118.6
10.0
0.323
0.047
0.0206
0.0010
48.52
2.35
0.122
0.018
131.5
6.4
267
36
121.0
7.7
0.301
0.051
0.0205
0.0011
48.90
2.63
0.109
0.019
130.4
6.7
252
39
120.5
7.4
0.292
0.048
0.0198
0.0011
50.51
2.81
0.111
0.018
126.2
6.9
242
36
117.5
8.1
0.399
0.064
0.0194
0.0012
51.55
3.19
0.155
0.027
123.9
7.6
312
46
107.4
9.2
0.341
0.060
0.0197
0.0015
50.76
3.87
0.148
0.030
125.4
9.2
277
45
114.0
11.0
0.357
0.059
0.0210
0.0016
47.62
3.63
0.134
0.028
133.6
10.0
284
43
123.0
11.0
0.374
0.054
0.0209
0.0015
47.85
3.43
0.154
0.027
133.2
9.5
313
42
119.0
11.0
0.301
0.056
0.0213
0.0014
46.95
3.09
0.117
0.024
135.6
8.8
243
42
125.7
10.0
vii
TESCHENITES FROM THE TYPE-LOCALITY IN THE OUTER WESTERN CARPATHIANS
GEOLOGICA CARPATHICA
, 2019, 70, 3, 222–240
Isotope ratios
Ages (Ma)
207
Pb/
235
U
±2SE
206
Pb/
238
U ±2SE
238
U/
206
Pb ±2SE
207
Pb/
206
Pb ±2SE
206
Pb/
238
U age
±2SE
207
Pb/
235
U age
±2SE
207
Pb-corr. Age ±2SE
0.200
0.026
0.0189
0.0008
52.94
2.13
0.078
0.010
120.6
4.8
182
23
117.3
5.6
0.759
0.072
0.0248
0.0013
40.32
2.11
0.232
0.024
157.7
8.0
555
43
123.1
10.0
0.151
0.015
0.0195
0.0006
51.36
1.64
0.057
0.006
124.3
3.9
142
13
122.8
4.5
0.378
0.070
0.0200
0.0013
50.00
3.25
0.143
0.030
127.5
8.5
291
49
115.0
11.0
0.360
0.068
0.0209
0.0014
47.85
3.21
0.139
0.028
133.1
9.1
295
50
119.0
11.0
0.386
0.061
0.0203
0.0013
49.26
3.15
0.151
0.027
129.7
8.5
306
42
115.3
9.8
0.758
0.064
0.0244
0.0011
40.98
1.85
0.228
0.020
155.4
6.8
557
38
121.1
7.8
0.285
0.057
0.0198
0.0014
50.51
3.57
0.108
0.022
126.2
8.6
242
43
116.3
9.3
0.367
0.062
0.0215
0.0013
46.51
2.81
0.124
0.021
137.2
8.1
291
44
123.6
9.5
0.416
0.069
0.0219
0.0015
45.66
3.13
0.151
0.025
139.7
9.5
336
49
123.0
11.0
0.519
0.057
0.0223
0.0012
44.84
2.41
0.174
0.019
142.4
7.3
406
37
121.4
7.7
0.362
0.066
0.0209
0.0014
47.85
3.21
0.133
0.026
133.2
8.7
289
48
121.4
10.0
0.419
0.065
0.0218
0.0016
45.87
3.37
0.147
0.024
138.9
10.0
327
46
123.2
10.0
0.363
0.058
0.0213
0.0016
46.95
3.53
0.143
0.024
135.0
10.0
290
42
122.0
12.0
0.389
0.085
0.0210
0.0017
47.62
3.85
0.152
0.039
134.0
11.0
317
61
118.0
13.0
0.326
0.057
0.0194
0.0013
51.55
3.45
0.143
0.027
123.7
8.5
274
44
110.9
10.0
Sample CJ-12
0.710
0.100
0.0236
0.0015
42.37
2.69
0.241
0.040
150.0
9.5
502
61
117.0
12.0
0.715
0.092
0.0241
0.0017
41.49
2.93
0.235
0.033
153.0
11.0
515
57
119.0
12.0
0.636
0.080
0.0238
0.0017
42.02
3.00
0.206
0.030
152.0
10.0
468
48
124.0
12.0
0.800
0.100
0.0250
0.0017
40.00
2.72
0.249
0.036
161.0
11.0
561
59
126.0
13.0
0.619
0.087
0.0245
0.0017
40.82
2.83
0.200
0.033
156.0
11.0
456
56
129.0
13.0
0.702
0.090
0.0239
0.0015
41.84
2.63
0.223
0.033
151.8
9.5
508
54
122.0
12.0
0.516
0.065
0.0237
0.0012
42.19
2.14
0.160
0.020
151.0
7.7
409
44
129.4
9.1
0.596
0.072
0.0243
0.0013
41.15
2.20
0.193
0.027
154.7
8.1
454
46
129.0
10.0
0.639
0.091
0.0232
0.0015
43.10
2.79
0.225
0.037
147.6
9.6
465
58
119.0
11.0
0.536
0.063
0.0230
0.0014
43.48
2.65
0.184
0.024
146.4
8.8
424
44
123.2
10.0
0.597
0.073
0.0240
0.0017
41.67
2.95
0.205
0.030
153.0
10.0
466
50
125.0
13.0
0.630
0.100
0.0234
0.0016
42.74
2.92
0.207
0.034
148.7
10.0
457
63
120.0
12.0
0.810
0.100
0.0248
0.0019
40.32
3.09
0.255
0.034
157.0
12.0
566
58
120.0
14.0
0.594
0.081
0.0238
0.0013
42.02
2.30
0.192
0.027
151.5
8.0
439
51
126.2
9.9
0.677
0.087
0.0260
0.0017
38.46
2.51
0.204
0.030
165.0
11.0
485
55
137.0
13.0
0.730
0.100
0.0242
0.0017
41.32
2.90
0.240
0.038
154.0
10.0
512
62
120.0
13.0
0.660
0.110
0.0238
0.0016
42.02
2.82
0.207
0.039
152.7
10.0
462
69
125.0
12.0
0.693
0.090
0.0241
0.0016
41.49
2.75
0.222
0.032
153.4
9.9
493
56
124.0
12.0
0.710
0.120
0.0271
0.0018
36.90
2.45
0.195
0.034
172.0
11.0
487
66
142.0
14.0
0.770
0.120
0.0248
0.0018
40.32
2.93
0.238
0.038
158.0
11.0
529
67
122.0
14.0
0.830
0.110
0.0255
0.0017
39.22
2.61
0.242
0.033
162.0
11.0
566
60
124.0
13.0
0.710
0.110
0.0252
0.0018
39.68
2.83
0.230
0.038
160.0
11.0
502
63
128.0
14.0
0.642
0.089
0.0255
0.0015
39.22
2.31
0.192
0.028
162.0
9.2
471
56
134.0
11.0
0.770
0.110
0.0235
0.0020
42.55
3.62
0.260
0.047
150.0
12.0
532
61
114.0
14.0
0.680
0.094
0.0231
0.0015
43.29
2.81
0.252
0.040
146.8
9.3
483
57
115.0
12.0
0.710
0.220
0.0245
0.0031
40.82
5.16
0.246
0.093
156.0
19.0
480
130
124.0
25.0
0.680
0.110
0.0241
0.0016
41.49
2.75
0.228
0.040
153.6
10.0
471
64
125.0
14.0
0.850
0.110
0.0262
0.0019
38.17
2.77
0.271
0.040
167.0
12.0
576
60
128.0
14.0
0.546
0.070
0.0240
0.0014
41.67
2.43
0.183
0.025
153.0
9.0
428
48
131.0
11.0
0.584
0.088
0.0236
0.0017
42.37
3.05
0.193
0.033
150.0
10.0
423
58
125.0
12.0
0.900
0.130
0.0260
0.0016
38.46
2.37
0.250
0.034
165.5
9.8
593
64
124.0
13.0
0.810
0.120
0.0264
0.0020
37.88
2.87
0.246
0.040
167.0
13.0
550
70
130.0
16.0
0.690
0.110
0.0245
0.0016
40.82
2.67
0.230
0.039
155.9
9.9
484
68
124.0
13.0
0.508
0.077
0.0238
0.0014
42.02
2.47
0.169
0.030
151.6
8.8
388
53
132.0
11.0
0.800
0.120
0.0254
0.0019
39.37
2.95
0.245
0.039
162.0
12.0
552
66
124.0
15.0
0.528
0.075
0.0246
0.0016
40.65
2.64
0.165
0.025
156.3
9.8
411
52
134.0
11.0
Table S2 (continued): Summary of laser ablation ICP-MS U–Pb titanite dating results.
viii
BRUNARSKA and ANCZKIEWICZ
GEOLOGICA CARPATHICA
, 2019, 70, 3, 222–240
Isotope ratios
Ages (Ma)
207
Pb/
235
U
±2SE
206
Pb/
238
U ±2SE
238
U/
206
Pb ±2SE
207
Pb/
206
Pb ±2SE
206
Pb/
238
U age
±2SE
207
Pb/
235
U age
±2SE
207
Pb-corr. Age ±2SE
0.710
0.130
0.0244
0.0025
40.98
4.20
0.231
0.050
155.0
16.0
513
83
123.0
18.0
Sample Czi-1-12
1.050
0.120
0.0272
0.0015
36.76
2.03
0.299
0.039
172.9
9.1
681
59
124.0
13.0
0.471
0.049
0.0220
0.0011
45.45
2.27
0.157
0.017
140.4
7.0
386
34
122.1
7.7
1.070
0.190
0.0258
0.0028
38.76
4.21
0.313
0.062
164.0
18.0
704
92
113.0
21.0
1.060
0.110
0.0277
0.0014
36.10
1.82
0.283
0.032
175.9
8.5
694
56
125.0
11.0
0.726
0.052
0.0234
0.0009
42.72
1.64
0.235
0.021
149.1
5.7
541
31
117.0
7.5
0.860
0.170
0.0243
0.0020
41.15
3.39
0.251
0.046
155.0
13.0
585
88
115.0
16.0
1.010
0.120
0.0260
0.0016
38.46
2.37
0.304
0.039
165.4
10.0
675
62
116.0
13.0
0.463
0.067
0.0215
0.0011
46.51
2.38
0.157
0.024
137.3
7.0
370
46
118.7
8.3
0.820
0.130
0.0238
0.0016
42.02
2.82
0.256
0.044
151.6
10.0
575
72
113.0
13.0
1.007
0.095
0.0264
0.0013
37.88
1.87
0.288
0.030
167.9
8.0
683
48
121.0
11.0
1.350
0.160
0.0275
0.0022
36.36
2.91
0.381
0.055
175.0
14.0
848
65
110.0
19.0
1.590
0.140
0.0314
0.0018
31.85
1.83
0.405
0.047
199.0
11.0
930
57
120.0
16.0
1.040
0.130
0.0271
0.0016
36.90
2.18
0.298
0.038
172.0
9.9
683
65
121.0
11.0
0.783
0.077
0.0244
0.0012
40.98
2.02
0.243
0.025
155.2
7.8
561
45
119.6
8.8
0.417
0.032
0.0208
0.0007
48.03
1.61
0.147
0.012
132.8
4.4
347
23
116.9
4.8
0.855
0.095
0.0266
0.0017
37.59
2.40
0.255
0.033
169.0
11.0
597
55
129.0
13.0
0.930
0.130
0.0266
0.0023
37.59
3.25
0.267
0.044
169.0
14.0
647
67
126.0
17.0
0.620
0.063
0.0241
0.0012
41.49
2.07
0.203
0.023
153.1
7.4
470
38
126.1
9.0
0.658
0.051
0.0242
0.0009
41.41
1.53
0.200
0.017
153.8
5.6
500
31
125.2
7.0
1.870
0.340
0.0368
0.0036
27.17
2.66
0.381
0.077
233.0
23.0
1010
120
139.0
33.0
0.857
0.085
0.0257
0.0011
38.91
1.67
0.246
0.026
163.6
7.0
600
46
125.2
8.7
1.070
0.150
0.0269
0.0017
37.17
2.35
0.316
0.051
171.0
11.0
692
73
120.0
15.0
0.589
0.073
0.0245
0.0014
40.82
2.33
0.178
0.024
155.7
8.6
473
53
129.7
9.7
0.761
0.084
0.0240
0.0014
41.67
2.43
0.243
0.027
153.0
8.9
551
49
117.2
9.6
0.980
0.110
0.0272
0.0016
36.76
2.16
0.278
0.036
172.6
9.8
647
59
127.0
12.0
1.040
0.100
0.0275
0.0016
36.36
2.12
0.298
0.036
175.0
10.0
692
50
127.0
12.0
0.707
0.085
0.0238
0.0014
42.02
2.47
0.223
0.030
151.5
8.9
525
54
120.0
11.0
0.762
0.079
0.0235
0.0015
42.55
2.72
0.251
0.028
149.4
9.2
553
47
114.0
10.0
1.460
0.160
0.0309
0.0020
32.36
2.09
0.350
0.036
196.0
12.0
858
71
123.0
12.0
0.619
0.063
0.0228
0.0010
43.80
1.92
0.209
0.025
145.5
6.4
470
40
118.6
8.4
0.742
0.086
0.0260
0.0015
38.46
2.22
0.232
0.037
165.1
9.3
545
52
132.0
13.0
0.946
0.096
0.0271
0.0014
36.90
1.91
0.273
0.032
172.3
8.9
656
54
126.0
12.0
0.984
0.094
0.0255
0.0013
39.22
2.00
0.310
0.038
162.1
8.1
664
49
115.0
11.0
0.880
0.110
0.0250
0.0019
40.00
3.04
0.260
0.035
159.0
12.0
612
59
118.0
13.0
1.140
0.110
0.0287
0.0017
34.84
2.06
0.324
0.041
182.0
11.0
751
55
127.0
15.0
0.564
0.048
0.0226
0.0008
44.23
1.58
0.191
0.019
144.1
5.1
446
31
118.5
6.7
0.712
0.079
0.0246
0.0012
40.65
1.98
0.220
0.026
156.7
7.3
529
48
123.8
9.1
0.738
0.065
0.0237
0.0012
42.19
2.14
0.236
0.023
151.1
7.2
546
40
117.0
8.4
Sample CBH1-12
0.688
0.068
0.0234
0.0011
42.74
2.01
0.227
0.025
148.7
6.6
500
41
119.3
8.3
1.137
0.086
0.0292
0.0013
34.25
1.52
0.303
0.027
185.4
8.2
742
43
131.0
10.0
0.715
0.072
0.0240
0.0012
41.67
2.08
0.226
0.024
152.9
7.8
522
44
119.2
8.9
0.128
0.025
0.0182
0.0007
54.91
2.17
0.049
0.010
116.3
4.5
115
21
115.9
5.1
0.265
0.042
0.0202
0.0010
49.58
2.34
0.099
0.016
128.6
6.0
231
33
120.2
6.8
0.830
0.098
0.0248
0.0014
40.32
2.28
0.262
0.034
157.7
8.9
583
55
119.0
11.0
0.822
0.057
0.0249
0.0009
40.16
1.39
0.244
0.019
158.5
5.4
594
32
120.7
6.4
0.566
0.076
0.0212
0.0014
47.17
3.11
0.198
0.029
135.4
8.6
431
51
110.0
10.0
1.317
0.093
0.0302
0.0013
33.11
1.43
0.337
0.029
191.7
8.4
837
41
126.0
11.0
0.676
0.076
0.0236
0.0012
42.37
2.15
0.228
0.030
150.1
7.5
510
48
118.8
9.7
0.561
0.074
0.0218
0.0013
45.87
2.74
0.182
0.027
139.2
8.1
428
47
115.4
9.9
0.803
0.082
0.0258
0.0013
38.76
1.95
0.250
0.030
163.8
7.9
572
50
126.0
10.0
Table S2 (continued): Summary of laser ablation ICP-MS U–Pb titanite dating results.
ix
TESCHENITES FROM THE TYPE-LOCALITY IN THE OUTER WESTERN CARPATHIANS
GEOLOGICA CARPATHICA
, 2019, 70, 3, 222–240
Isotope ratios
Ages (Ma)
207
Pb/
235
U
±2SE
206
Pb/
238
U ±2SE
238
U/
206
Pb ±2SE
207
Pb/
206
Pb ±2SE
206
Pb/
238
U age
±2SE
207
Pb/
235
U age
±2SE
207
Pb-corr. Age ±2SE
1.020
0.110
0.0270
0.0015
37.04
2.06
0.285
0.032
171.8
9.3
685
57
124.0
12.0
3.270
0.240
0.0482
0.0023
20.75
0.99
0.499
0.041
303.0
14.0
1440
60
140.0
19.0
0.555
0.046
0.0219
0.0008
45.60
1.66
0.186
0.017
139.8
5.0
434
30
116.3
5.7
0.576
0.077
0.0229
0.0013
43.67
2.48
0.204
0.029
145.7
8.1
433
50
120.2
8.8
0.646
0.068
0.0226
0.0011
44.25
2.15
0.231
0.030
143.8
7.0
488
43
115.3
9.1
0.127
0.019
0.0191
0.0006
52.25
1.56
0.049
0.007
122.2
3.6
117
16
121.7
4.0
4.250
0.230
0.0560
0.0023
17.86
0.73
0.559
0.036
351.0
14.0
1664
46
131.0
20.0
0.599
0.066
0.0216
0.0010
46.30
2.14
0.212
0.025
137.7
6.4
448
42
112.3
7.6
0.215
0.029
0.0192
0.0008
52.16
2.18
0.084
0.012
122.3
5.0
188
24
117.3
5.5
1.370
0.120
0.0291
0.0014
34.36
1.65
0.353
0.037
184.6
9.0
852
53
117.0
12.0
0.468
0.064
0.0216
0.0012
46.30
2.57
0.174
0.026
137.5
7.3
371
46
117.1
8.5
0.528
0.061
0.0226
0.0012
44.25
2.35
0.190
0.026
144.2
7.3
404
42
122.5
9.1
0.817
0.061
0.0236
0.0009
42.30
1.61
0.262
0.022
150.5
5.7
590
35
113.1
7.2
Sample CR6-11
0.416
0.047
0.0218
0.0010
45.79
2.10
0.145
0.018
139.1
6.4
335
34
123.3
7.1
0.401
0.067
0.0214
0.0013
46.73
2.84
0.156
0.032
136.6
8.0
312
48
120.4
9.8
0.577
0.068
0.0224
0.0011
44.64
2.19
0.204
0.026
142.8
7.0
436
45
117.0
9.1
0.482
0.069
0.0218
0.0013
45.87
2.74
0.165
0.025
138.7
8.1
369
48
118.1
9.2
0.377
0.046
0.0214
0.0009
46.82
2.06
0.132
0.017
136.1
6.0
315
35
120.7
6.7
0.495
0.054
0.0215
0.0009
46.45
2.01
0.177
0.021
137.9
6.0
391
37
117.0
7.4
0.366
0.045
0.0214
0.0010
46.82
2.19
0.134
0.018
136.1
6.3
299
34
123.0
7.3
0.249
0.031
0.0192
0.0009
52.16
2.34
0.103
0.013
122.3
5.4
223
26
114.6
6.1
0.396
0.064
0.0219
0.0012
45.66
2.50
0.141
0.026
139.8
7.6
314
47
124.0
8.9
0.329
0.053
0.0201
0.0010
49.75
2.48
0.138
0.024
128.3
6.6
262
40
118.0
8.5
0.345
0.051
0.0207
0.0010
48.31
2.33
0.127
0.020
132.2
6.5
271
37
120.4
7.4
0.298
0.045
0.0211
0.0011
47.39
2.47
0.112
0.019
134.5
7.1
244
35
125.1
8.1
0.351
0.047
0.0212
0.0010
47.19
2.16
0.126
0.018
135.0
6.1
282
34
123.9
7.6
0.364
0.061
0.0206
0.0013
48.54
3.06
0.147
0.026
131.1
7.9
292
46
116.9
9.1
0.674
0.065
0.0225
0.0010
44.42
1.87
0.225
0.022
143.4
6.0
498
39
112.6
6.9
0.442
0.073
0.0204
0.0014
49.02
3.36
0.165
0.032
130.0
8.7
339
50
112.0
10.0
0.400
0.057
0.0204
0.0011
49.02
2.64
0.155
0.025
129.8
7.1
318
41
112.8
8.1
Table S2 (continued): Summary of laser ablation ICP-MS U–Pb titanite dating results.