GeolCarp_Vol69_No5_453

GEOLOGICA CARPATHICA

, OCTOBER 2018, 69, 5, 453–466

doi: 10.1515/geoca-2018-0026

www.geologicacarpathica.com

Petrology and dating of the Permian lamprophyres from

the Malá Fatra Mts. (Western Carpathians, Slovakia)

JÁN SPIŠIAK

, LUCIA VETRÁKOVÁ

, DAVID CHEW

, ŠTEFAN FERENC

, TOMÁŠ MIKUŠ

VIERA ŠIMONOVÁ

and PETER BAČÍK

3, 4

Faculty of Natural Sciences, Matej Bel University, Tajovského 40, 974 01 Banská Bystrica, Slovakia; jan.spisiak@umb.sk

Department of Geology, Trinity College Dublin, Dublin 2, Ireland

Earth Science Institute, Slovak Academy of Sciences, Dúbravská cesta 9, 840 05 Bratislava, Slovakia

Department of Mineralogy and Petrology, Faculty of Natural Sciences, Comenius University in Bratislava, Ilkovičova 6,

842 15 Bratislava, Slovakia

(Manuscript received November 3, 2017; accepted in revised form October 4, 2018)

Abstract: Calc–alkaline lamprophyres are known from several localities in the Malá Fatra Mountains. They form dykes

(0.5–3 m) of varying degree of alteration that have intruded the surrounding granitoid rocks which are often incorporated

xenoliths. Clinopyroxenes (diopside to augite), amphiboles (kaersutitic), biotites (annite) and plagioclases are major

primary minerals of the dykes, accessory minerals include apatite, ilmenite, rutile, pyrite, chalcopyrite, and pyrrhotite.

Apatite has a relatively low F, but increased Cl content compared to typical apatite from lamprophyres or magmatic

apatite from granitic rocks in the Western Carpathians. The chemical composition of the lamprophyres indicates

their calc–alkaline character, but affinity to alkaline lamprophyres is suggested by the Ti enrichment in clinopyroxene,

amphibole and biotite. According to modal classification of the minerals, the studied rocks correspond to spessartite.

The differences in the chemical composition of the rocks (including Sr and Nd isotopes) probably result from the contami-

nation of primary magma by crustal material during magma ascent. The age of the lamprophyres, based on U/Pb dating

in apatite, is 263.4 ± 2.6 Ma.

Keywords: calc–alkaline lamprophyres, mineralogy, geochemistry, Malá Fatra Mts.

Introduction

Lamprophyres are dyke rocks which differ from intrusive and

effusive rocks in mineral composition, structure and, to some

degree, chemical composition. The term lamprophyre was

introduced by Gümbel (1874) to denote dark-coloured dyke

rocks of variable mineral composition.

Lamprophyres are generally ultramafic, mafic, or interme-

diate rocks that intrude the basement at shallow-crustal levels

and form dykes or sills. They are porphyritic rocks comprising

phenocrysts of mafic minerals in a groundmass consisting of

the same early crystallized minerals. The early magmatic

mafic minerals include phlogopite, olivine, amphibole, clino-

pyroxene, and apatite (Bergman 1987; Rock 1987, 1991).

The lamprophyric magmas are typically formed at low degrees

of partial melting of an upper mantle source at a depth of

100–150 km (Rock 1991). These magmas are known to have

very high concentrations of volatiles (F, CO

, H

O) and incom-

patible trace elements (light REE, Zr, Sr, Ba). Such high vola-

tile contents likely result either from a previously volatile and

incompatible elements-rich mantle source (Ulrych et al. 1993)

or from fluid-rich metasomatism (McKenzie 1989). Lampro-

phyres cannot be simply referred to as textural varieties of

common plutonic or volcanic rocks, they are more complex in

nature (Seifert 2005). They are hybrid rocks, resulting from

interactions of mantle melts with more evolved crustal

material by processes of magma mixing (mafic–felsic melts)

and/or assimilation of country-rock material (Rock 1991).

In the crystalline complexes of the Western Carpathians,

lamprophyres occur in various core mountains: Považský

Inovec Mts., Suchý Mts., Malá Fatra Mts., Nízke Tatry Mts.,

but they are also known from the Veporic complexes (Hovorka

1967). Yet no attention has been paid to the detailed mine-

ralogical and geochemical characteristics and age of these

rocks. The focus of this work is on the detailed study of

the mineral composition and geochemistry of Malá Fatra Mts.

lamprophyres.

Geological setting

Basic dyke rocks from the Malá Fatra Mts. were first

described by Ivanov and Kamenický (1957) from the area of

the Kriváň hill (elevation Veľká Kráľová) and Martinské hole

Mountains. The rocks occur as dykes of different thickness

(0.5–3 m). Hovorka (1967) labelled these rocks as monsonitic

lamprophyres. Lamprophyres are found in the surroundings of

granitoid rocks (granodiorite and tonalite) of the Western

Carpathians crystalline complexes. Some of the Malá Fatra

lamprophyre dykes were relatively strongly tectonically

affected, which indicates their pre-Alpine age. Depending

on the structure, texture and mineral composition of

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GEOLOGICA CARPATHICA

, 2018, 69, 5, 453–466

lamprophyres, several types of dyke rocks can be distin-

guished in the Malá Fatra Mts.: porphyric, equigranular and

amygdaloidal. Lamprophyres were studied from two localities

(Fig. 1):

• Outcrops of dykes at the cable car valley station at Martinské

hole near Kalužná hill (49°5’49” N, 18°50’28” E).

• Dykes in Dubná skala granite quarry (49°8’25” N,

18°52’43” E) and dykes from the Višňové highway tunnel

gallery.

The studied lamprophyres often contain xenoliths of

the surrounding granitoid rocks and their minerals resorbed

in a different stage. The surrounding granitoid rocks have

the charac ter of hybrid tonalities (Kamenický et al. 1987) or

I-type granites (Broska et al. 1997). The minerals represented

in the rocks are mainly plagioclases (oligoclase–andesine),

strongly undulosed quartz, less potassium feldspar and bio-

tites, and relatively rarely muscovite.

Mesozoic sequences of the Malá Fatra also contained

Cretaceous alkaline lamprophyres (Polom, Višňové or

Krpeľany; Hovorka & Spišiak 1988; Spišiak 1999). They are

different in age, mineral and chemical composition, but above

all, in the presence of foids and absence of quartz and

feldspar.

Analytical methods

Silicates and apatites were studied using electron micro-

probe JEOL JXA 8530FE at the Earth Sciences Institute of

the Slovak Academy of Sciences in Banská Bystrica under

the following conditions for silicates: accelerating voltage

15 kV, probe current 20 nA, beam diameter 3–8 µm, ZAF

correction, counting time 10 s on peak, 5 s on background.

The used standards, X-ray lines and D.L. (in ppm) were:

Ca(Kα, 25) — diopside; K (Kα, 44) —

orthoclase; P (Kα, 41) — apatite; F (Kα,

167) — fluorite; Na (Kα, 43) — albite;

Mg (Kα, 41) — diopside; Al (Kα, 42)

— albite; Si (Kα, 63) — quartz; Ba (Lα,

72) — barite; Fe (Kα, 52) — hematite;

Cr (Kα, 113) — Cr

; Mn (Kα, 59) —

rhodonite; Ti (Kα, 130) — rutile; Cl

(Kα, 12) — tugtupite; Sr (Lα, 71) —

celestite. The following conditions for

apatites were used: accelerating voltage

15 kV, probe current 20nA and beam

diameter 5 μm and ZAF matrix correc-

tion was used. The EPMA was cali-

brated by the natural and synthetic

standards. Used standards, X-ray lines,

crystal and D.L. (in ppm) are:

Ca (Kα, PETL, 24–62) — diopside;

K (Kα, PETL, 20–48) — orthoclase;

Th (Mα, PETL, 41–75) — thorianite;

Pb (Mβ, PETL, 65–138) — crocoite;

Cl (Kα, PETL, 11–12) — tugtupite;

P (Kα, PETL, 56–85) — apatite; S (Kα,

PETL, 27–47) — barite; Y — (Lα,

PETL, 59–122) — YPO

; F (Kα, LDE1,

103–273) — fluorite; Na (Kα, TAP,

46–78) — albite; Sr (Lα, TAP, 38–201)

— celestite; Si (Kα, TAP, 50–125) —

orthoclase; Al (Kα, TAP, 37–100) —

albite; Mg (Kα, TAP, 37–87) — diopside;

Sm (Lβ, LIFH, 62–274) — SmPO

;

Pr (Lβ, LIFH, 121–235) — PrPO

;

Nd (Lα, LIFH, 62–123) — NdPO

;

Ce (Lα, LIFH, 65–129) — CePO

;

La (Lα, LIFH, 72–139) — LaPO

;

Fe (Kα, LIF, 94–333) — hematite;

Mn (Kα, LIF, 79–238) — rhodonite;

Ti (Kα, LIF, 133–333) — rutile; Ba (Lα,

LIF, 242–674) — barite.

Fig. 1. Geological map of part of Malá Fatra Mts. (Digital geological map of the Slovak

Republic at scale 1:50,000 [online].

State Geological Institute of Dionýz Štúr,

Bratislava,

2013).

Legend: 1 — fluvial sediments (Quaternary); 2 — proluvial sediments (Quaternary);

3 — deluvial sediments (Quaternary); 4 — Martin Fm. (calcareous clays, sandstones, con-

glomerates, Quaternary); 5 — Dubná Skala Fm. (nonsaline limestones, travertines, alms, con-

glomerates, Miocene); 6 — Mráznica Fm. (grey and dark-gray marly limestones, alms,

marlestones, Late Jurassic–Early Cretaceous); 7 — Allgäu Fm. (Early Jurassic);

8 — Guttenstein Limestones (Middle Triassic); 9 — Lúžna Fm. (Early Triassic); 10 — porfy-

rites, porphyrites, lamprophyres (Late Paleozoic); 11 — granites and granodiorites (Early

Paleozoic); 12 — amphibolites (Early Paleozoic); 13 — orthogneisses (Early Paleozoic);

14 — garnet–biotite paragneisses (Early Paleozoic); 15 — granodiorites and tonalities (Early

Paleozoic); 16 — fault lines; 17 — tectonic structure (nappe structure); 18 — samples.

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LAMPROPHYRES FROM MALÁ FATRA MTS. (WESTERN CARPATHIANS, SLOVAKIA)

GEOLOGICA CARPATHICA

, 2018, 69, 5, 453–466

The chemical composition of the rocks was determined at

the ACME Analytical Laboratories (Vancouver, Canada).

Total abundances of major element oxides were determined by

inductively coupled plasma–emission spectrometry (ICP-ES)

following lithium metaborate–tetraborate fusion and dilute

nitric acid treatment. Loss on ignition (LOI) was calculated

from the difference in weight after ignition to 1000 °C. For

the total carbon (TOT/C) and sulphur analysis (TOT/S) by

LECO analysis, the samples were heated in an induction fur-

nace to >1650 °C, which caused volatilization of all C and S

bearing phases. Vapours were carried through an infrared

spectrometric cell wherein the concentrations of C and S

were determined by the absorption of specific wavelengths

in the infrared spectra (ORG/C = TOT/C minus graphite C

and carbonate). Concentrations of trace elements and rare

earth elements were determined by ICP mass spectrometry

(ICP-MS). Further details are accessible on the web page of

the ACME Analytical Laboratories (http://acmelab.com/).

Apatite crystals were separated using standard techniques.

Apatite U–Pb data were acquired using a Photon Machines

Analyte Exite 193 nm ArF Excimer laser-ablation system

coupled to a Thermo Scientific iCAP Qc at the Department

of Geology Trinity College Dublin. Twenty-eight isotopes

(

Cl,

Ca,

Mn,

Sr,

139

La,

140

Ce,

141

Pr,

146

Nd,

147

Sm,

153

Eu,

157

Gd,

159

Tb,

163

Dy,

165

Ho,

166

Er,

169

Tm,

172

Yb,

175

Lu,

200

Hg,

204

Pb,

206

Pb,

207

Pb,

208

Pb,

232

Th,

238

U and mass

248

(

232

were acquired using a 50 μm laser spot, a 4 Hz laser repetition

rate and a fluence of 3.31 J/cm

. A ca. 1 cm sized crystal of

Madagascar apatite which has yielded a weighted average

ID-TIMS concordia age of 473.5 ± 0.7 Ma (Thomson et al.

2012; Cochrane et al. 2014) was used as the primary apatite

reference material in this study. McClure Mountain syenite

apatite (the rock from which the

Ar/

Ar hornblende standard

MMhb is derived) was used as a secondary standard. McClure

Mountain syenite has moderate but reasonably consistent U

and Th contents (~23 ppm and 71 ppm; Chew & Donelick

2012) and its thermal history, crystallization age (weighted

mean

207

Pb/

235

U age of 523.51 ± 2.09 Ma) and initial Pb isoto-

pic composition (

206

Pb/

204

Pb = 17.54 ± 0.24;

207

Pb/

204

Pb = 15.47

± 0.04) are known from high-precision TIMS analyses

(Schoene & Bowring 2006). Durango apatite was also ana-

lysed in this study as a secondary standard. Durango apatite is

a distinctive yellow-green fluorapatite widely used as a mine-

ral standard in apatite fission-track and (U–Th)/He dating and

apatite electron micro-probe analyses. It is found as large crys-

tals within an open pit iron mine at Cerro de Mercado,

Durango, Mexico. The apatite was formed between the erup-

tions of two major ignimbrites which have yielded a sanidine–

anorthoclase

Ar–

Ar age of 31.44 ± 0.18 Ma (McDowell et

al. 2005). NIST 612 standard glass was used as the apatite

trace element concentration reference material. The raw iso-

tope data were reduced using the “VizualAge” data reduction

scheme of Petrus & Kamber (2012) within the freeware

IOLITE package of Paton et al. (2011). User-defined time

intervals are established for the baseline correction procedure

to calculate session-wide baseline-corrected values for each

isotope. The time-resolved fractionation response of indivi-

dual standard analyses is then characterized using a user-

speci fied down-hole correction model (such as an exponential

curve, a linear fit or a smoothed cubic spline). The data reduc-

tion scheme then fits this appropriate sessionwide “model”

U–Th–Pb fractionation curve to the time-resolved standard

data and the unknowns. Sample-standard bracketing is applied

after the correction of down-hole fractionation to account for

long-term drift in isotopic or elemental ratios by normalizing

all ratios to those of the U–Pb reference standards. Common

Pb in the apatite standards was corrected using the

207

Pb-based

correction method using a modified version of the VizualAge

DRS that accounts for the presence of variable common Pb

in the primary standard materials (Chew et al. 2014). Over

the course of two months of analyses, McClure Mountain apa-

tite (

207

Pb/

235

U TIMS age of 523.51 ± 1.47 Ma; Schoene &

Bowring 2006) yielded a U–Pb Tera-Wasserburg concordia

lower intercept age of 524.5 ± 3.7 Ma with an MSWD = 0.72.

The lower intercept was anchored using a

207

Pb/

206

Pb value of

value of 0.88198 derived from an apatite ID-TIMS total U–Pb

isochron (Schoene & Bowring 2006).

Samples for Sr and Nd isotope analyses were chemically

prepared and measured in the Isotope Geochemistry

Laboratory in the Institute of Geological Sciences of the Polish

Academy of Science, Krakow. The analyses were made with

a Multi-Collector Inductively Coupled Plasma Mass

Spectrometer (MC-ICP-MS) Neptune. The samples were

digested in three steps: firstly, with HF : HNO

, secondly, with

HNO

and finally, with HCl and HF, following the procedure

described by Anczkiewicz et al. (2004) and Anczkiewicz &

Thirlwall (2003). The samples were then dissolved in HCl for

loading on cation exchange columns with AG50Wx8 resin

(Anczkiewicz et al. 2004). Final separation of Sr was per-

formed by Sr-spec resin (Peryt et al. 2010) and Nd by Ln-spec

resin (Anczkiewicz & Thirlwall 2003). Nd isotopes were

normalized to

143

Nd/

144

Nd = 0.7219 to correct for mass bias.

The reproducibility of Nd standards over the period of analy-

ses was

143

Nd/

144

Nd = 0.512101 ± 8 (2 s.d. n = 3). Sr isotopes

were normalized to

Sr/

Sr = 0.1194 to correct for mass bias.

The reproducibility of Sr standards over the period of analyses

was

Sr/

Sr = 0.710261 ± 8 (2 s.d. n = 3). They were also

chemi cally prepared and measured in the Isotope Geochemistry

Laboratory in the Institute of Geological Sciences of the Polish

Academy of Science, Krakow. The εNd(0,t) values were

calculated with parameters for CHUR

143

Nd/

144

Nd = 0.512638,

147

Sm/

144

Nd = 0.1967 (Jacobsen & Wasserburg 1980; DePaolo

1981).

Results

Petrographic observation

Lamprophyres from the Malá Fatra Mountains are pale

green, grey-green to dark grey in colour and they mostly have

porphyric texture (equigranular types are less frequent), rarely

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GEOLOGICA CARPATHICA

, 2018, 69, 5, 453–466

also amygdaloidal texture. Phenocrysts are formed by plagio-

clase, quartz, pyroxene, biotite, rarely also amphibole. In some

places, there are occurrences of irregular, up to 6 cm large

xenoliths of the surrounding granitoid rocks or their minerals

(mainly plagioclases; Fig. 2a). Oval-shaped amygdales filled

with carbonate, rarely with chlorite are also frequent (Fig. 2b).

The rocks are characterized by strongly, usually almost com-

pletely altered primary minerals, namely clinopyroxenes, but

often also amphiboles and biotites. This is the reason for diffi-

culties in the classification of rocks based on their modal

mineral composition composition (Spišiak & Hovorka 1998).

Nevertheless, based on the observed relics of minerals, their

pseudomorphoses and types of alte rations, the studied rocks

correspond to spessartite. The chemi cal and isotopic composi-

tions of the lamprophyres from the Malá Fatra Mts. in

the analysed samples are given in Tables 1 and 2.

We determined the age of the rocks using LA-ICP-MS

by apatite analysis (Trinity College, Dublin, Ireland) as

263.4 ± 2.6 Ma (Fig. 3), which corresponds well to their geo-

logical position.

Mineralogical characterization

Clinopyroxenes usually form phenocrysts with a typical

oscillatory and sector (hour-glass texture) (Fig. 4a) zoning.

The pyramidal sector is enriched with SiO

and MgO, or

depleted in TiO

, Al

and Na

O compared to the prismatic

sector (Table 3). The studied clinopyroxenes are characterized

by relatively high contents of TiO

and Na

O. Based on the

IMA classification of pyroxenes (Morimoto et al. 1988), they

Fig. 2. a — Photo of the lamprophyres structure; light irregular shape

— xenolith of the surrounded granitoids, small ovoid-shape carbonate

amygdaloids; b — photomicrograph of carbonate amygdales, crossed

polaroids.

MH-1

MH-2

DS-55

DS-424

SiO

39.96

46.85

53.22

48.10

TiO

1.65

1.85

1.63

1.75

14.05

16.64

15.68

15.92

9.88

10.68

8.44

9.97

0.02

0.03

MnO

0.16

0.18

0.08

0.16

MgO

6.55

5.38

7.23

6.88

CaO

9.40

4.76

1.77

6.36

3.24

3.20

4.39

2.95

1.82

3.59

1.34

1.63

0.60

0.66

0.46

0.44

LOI

12.30

5.80

5.50

Total

99.63

99.73

99.76

99.73

TOT/C

2.91

0.83

0.27

0.51

TOT/S

0.08

0.07

0.06

433

1052

308

425

27.8

27.9

18.6

33.7

1.5

1.7

1.4

1.6

13.6

16.1

15.6

4.9

5.5

5.4

5.1

53.8

66.2

53.1

47.3

41.1

60.3

20.5

36.7

571.7

589.4

113.9

509.3

3.4

4.1

3.4

3.0

4.5

5.7

5.8

5.9

2.3

117

128

139

158

0.7

0.5

1.3

219

273.5

241.4

220.9

21.3

25.7

22.8

24.5

39.9

50.1

33.7

37.7

79.6

87.7

69.2

8.69

10.04

7.71

8.17

32.2

36.8

28.2

31.3

5.45

6.37

5.28

6.14

1.83

1.97

1.59

1.7

5.18

5.73

5.2

5.47

0.74

0.84

0.7

0.8

4.3

4.6

4.17

4.64

0.77

0.95

0.79

0.9

2.16

2.67

2.28

2.49

0.32

0.38

0.34

0.37

1.98

2.48

2.24

0.32

0.35

0.37

Table 1: Chemical composition of lamprophyres from the Malá

Fatra Mts.

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, 2018, 69, 5, 453–466

can be classified as diopside to Ca-rich augite (Fig. 5). There

are also rare occurrences of clinopyroxene xenocrysts in these

rocks (Fig. 4b). They are partially altered to form a mixture of

chlorite and hydrated grossular-andradite garnet. This altera-

tion must have taken place at the lamprophyres magma gene-

rating site, as the rims of the xenocrysts were formed later.

Compared to the phenocrysts, the xenocrysts have increased

contents of Al

, Na

O and TiO

and lower contents of SiO

and CaO (Table 3). The newly formed rims of xenocrysts have

a similar composition to the central part of phenocrysts.

An identical type of clinopyroxenes alteration was also

described in the Nízke Tatry Mountains Permian basalts

(Spišiak et al. 2017).

Amphibole is a relatively rare mineral (Fig. 6a) and is often

strongly altered. It usually has elevated contents of TiO

, Na

and K

O (Table 4). Based on the classification of amphiboles

(Hawthorne et al. 2012), it corresponds to kaersutitic amphi-

bole based on the Ti > 0.5 apfu. However, unknown Fe

/Fe

and (OH)

−

2−

ratio prevents exact classification. The Al con-

tent is too low for kaersutite. If a part of Fe is treated as triva-

lent to charge balance octahedral sites, amphibole would have

the composition of ferri-kaersutite. In contrast, if the charge at

octahedral sites is balanced by OH, the composition would be

between ferro-ferri-kaersutite and hastingsite. Like amphi-

bole, biotite is also strongly altered (chloritized). It is charac-

terized by the high content of TiO

, which documents its

magmatic origin (Table 4). Based on the mica classification of

Rieder et al. (1998), it corresponds to annite (Fig. 7). Abdel-

Rahman (1993) used the dependence of Al

and MgO in

biotites from different lamprophyre types for their genetic

classification. In the discrimination diagram (Fig. 8), the bio-

tites from the rocks under study are lying in the field of biotites

from calc–alkaline lamprophyres.

Plagioclase and K-feldspar are common felsic minerals in

these rocks, with plagioclase prevailing over alkaline feldspar.

Plagioclase has a relatively high basicity — An

(Table 5,

Fig. 6b). Strongly resorbed xenoliths of the surrounding gra-

nitoid rocks, and/or feldspar rarely occur. In plagioclase

xenocrysts, the original composition is often preserved only in

Age

143

Nd/

144

2SE

143

Nd/

144

Ndi

EpsNdi

Sr/

2SE

Sr/

Sri

DS-424

260

0.512725

0.000006

0.512523

4.29

0.705136

0.000008

0.704365

DS-55

260

0.5127624

0.000009

0.5127

5.2

0.707219

0.000011

0.705292

MH-1

260

0.512817

0.000005

0.512643

6.63

0.704381

0.000007

0.703612

MH-2

260

0.512813

0.000006

0.512635

6.47

0.704406

0.000008

0.703311

Table 2: Sr and Nd isotope composition of studied lamprophyres.

Fig. 3. LA-ICP-MS U–Pb age for apatite from studied lamprophyres.

Fig. 4. a, b — Back scattered electron (BSE) images of clinopy-

roxenes; HG — hydrated garnet, Chl — chlorite; the numbers in figures

correspond to those in Table 3.

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the central parts (basicity corresponds to the original granitoid

plagioclase; An

(Broska et al. 1997, Fig. 6b) and the rims are

replaced by more basic plagioclase. The rims (An

58–61

) of

the xenoliths correspond to primary plagioclase from lampro-

phyres (Fig. 9). K-feldspar is less common and has elevated

contents of Na

O and Ba (Table 5).

From the accessory minerals, apatite is the most common.

It forms columnar grains, or grains with a hexagonal shape

(Fig. 10a). Needle-like apatite (Fig. 6a) as well as oval-shape

apatite are observed in rare cases (Fig. 10b). According to their

composition (Fig. 10c, d; Table 6), the apatite studied here

belongs to the apatite group (Pasero et al. 2010) with the com-

position of hydroxylapatite. It has a low proportion of substi-

tuting cations (Fe < 0.04 apfu, Mg < 0.02 apfu, Na < 0.03 apfu,

N. anal.

Sector

SiO

46.33

49.96

48.29

50.04

50.27

50.36

47.03

47.29

47.04

47.06

49.18

47.96

48.70

49.29

50.77

TiO

2.97

1.67

2.28

1.60

1.41

1.45

1.82

1.83

1.86

1.89

2.26

1.99

1.95

1.52

6.41

2.81

4.44

2.84

3.15

2.78

8.34

8.40

8.53

8.62

4.02

4.73

3.73

4.19

2.98

0.29

0.01

0.00

0.31

0.27

0.02

0.01

0.04

0.03

0.04

0.14

0.04

0.07

0.08

3.34

2.10

2.74

2.91

1.92

1.41

3.21

3.02

2.42

2.77

2.49

4.30

3.05

2.45

1.81

FeO

5.47

7.16

7.18

6.36

6.49

6.69

5.62

5.93

6.41

6.17

4.79

6.19

6.53

6.86

MnO

0.17

0.27

0.31

0.25

0.26

0.24

0.20

0.22

0.23

0.18

0.21

0.22

0.19

0.28

0.23

MgO

12.40

13.83

12.35

14.15

14.79

14.65

12.92

12.90

12.71

12.87

13.27

13.33

13.28

13.42

14.22

CaO

21.57

21.37

21.58

21.24

20.78

20.97

19.26

19.28

19.17

19.06

21.89

21.77

21.64

21.36

21.61

0.56

0.37

0.55

0.46

0.34

0.91

0.93

0.85

0.90

0.51

0.56

0.47

0.54

0.40

0.03

0.02

0.03

0.02

0.01

0.04

0.01

0.03

0.02

0.04

0.02

0.03

Total

99.55

99.57

99.74

99.88

99.74

99.17

99.37

99.82

99.26

99.54

99.69

100.10

99.31

100.11

100.51

1.743

1.875

1.819

1.869

1.873

1.886

1.754

1.756

1.758

1.752

1.841

1.791

1.835

1.838

1.881

0.257

0.124

0.181

0.125

0.127

0.114

0.246

0.244

0.242

0.248

0.159

0.208

0.165

0.162

0.119

2.000

1.999

2.000

1.994

2.000

1.999

2.000

0.084

0.047

0.065

0.045

0.040

0.041

0.051

0.052

0.053

0.063

0.056

0.055

0.042

0.028

0.000

0.016

0.000

0.011

0.009

0.121

0.124

0.133

0.131

0.019

0.000

0.022

0.011

0.095

0.059

0.078

0.082

0.054

0.040

0.090

0.084

0.068

0.078

0.070

0.121

0.087

0.069

0.050

0.009

0.000

0.009

0.008

0.001

0.000

0.001

0.004

0.001

0.002

0.696

0.774

0.693

0.788

0.821

0.818

0.718

0.714

0.708

0.714

0.741

0.742

0.746

0.785

0.090

0.120

0.148

0.085

0.065

0.084

0.019

0.026

0.038

0.024

0.116

0.069

0.110

0.106

0.108

1.000

0.083

0.105

0.078

0.113

0.137

0.126

0.156

0.158

0.162

0.168

0.077

0.080

0.085

0.097

0.105

0.005

0.009

0.010

0.008

0.006

0.007

0.006

0.007

0.006

0.009

0.007

0.870

0.859

0.871

0.850

0.829

0.842

0.770

0.767

0.760

0.878

0.871

0.873

0.853

0.858

0.041

0.027

0.040

0.033

0.025

0.066

0.067

0.062

0.065

0.037

0.041

0.034

0.039

0.029

0.001

0.000

0.002

0.000

0.001

0.002

0.001

1.000

1.001

1.000

1.006

1.000

1.001

1.000

38.32 % 40.92 % 40.32 % 40.46 % 38.98 % 40.08 % 32.03 % 31.94 % 32.05 % 31.44 % 40.97 % 39.40 % 40.60 % 39.67 % 40.84 %

38.24 % 40.48 % 37.07 % 41.40 % 43.18 % 42.64 % 40.02 % 39.69 % 39.35 % 39.76 % 39.27 % 40.25 % 39.61 % 39.66 % 41.05 %

9.46 % 11.76 % 12.08 % 10.44 % 10.63 % 10.92 %

9.77 % 10.24 % 11.14 % 10.69 % 10.24 %

8.11 % 10.36 % 10.82 % 11.11 %

1.12 %

0.91 %

1.21 %

1.38 %

0.72 %

0.63 %

1.45 %

1.39 %

1.05 %

1.23 %

1.11 %

1.62 %

1.25 %

1.13 %

0.84 %

3.37 %

1.91 %

3.08 %

2.12 %

1.86 %

1.94 %

5.89 %

6.05 %

5.80 %

6.00 %

2.81 %

2.78 %

2.39 %

3.02 %

2.16 %

Ca–Ts

4.87 %

1.57 %

2.78 %

1.84 %

2.54 %

1.66 %

8.01 %

7.86 %

7.75 %

7.98 %

2.77 %

4.40 %

2.80 %

2.79 %

1.78 %

Ti–Ts

4.62 %

2.47 %

3.45 %

2.36 %

2.08 %

2.13 %

2.84 %

2.86 %

2.90 %

2.82 %

3.44 %

3.00 %

2.91 %

2.21 %

Fig. 5. Classification diagram of clinopyroxenes (Morimoto et al.

1988); D — diopside, H — hedenbergite, A — augite; pr — prismatic

sector, py — pyramidal sector, c — core, r — rims, xe — xenocryst.

Table 3: Selected analyses of clinopyroxenes. Crystal-chemical formula calculated based on 6 cations and Fe

/Fe

ratio calculated from

charge-balanced formula. pr — prismatic sector, py — pyramidal sector, c — core, xe — xenocryst, r — rims.

459

LAMPROPHYRES FROM MALÁ FATRA MTS. (WESTERN CARPATHIANS, SLOVAKIA)

GEOLOGICA CARPATHICA

, 2018, 69, 5, 453–466

REE < 0.03 apfu) but (OH)

−

is significantly substituted by F

−

(0.37–0.44 apfu) and Cl

−

(0.05 apfu).. From the opaque mine-

rals, the most common are ilmenite, rutile, pyrite, chalcopyrite,

pyrrhotite, while the sulphides are younger than the oxides.

Discussion

Geochemical characterization of the lamprophyres

The chemical composition of the lamprophyres from

the Malá Fatra Mts. can be used to reveal their genetic condi-

tions, although it is strongly affected by the alteration of these

rocks and amygdales and xenoliths of the surrounding grani-

toid rocks (or plagioclases) presence. In the classification

diagram of different types of lamprophyre rocks (Rock 1987),

the studied lamprophyres correspond to the calc–alkaline type

(Fig. 11). To compare, we plotted the average compositions of

calc–alkaline lamprophyres, spessartites (Rock 1991) and

Cretaceous alkaline lamprophyres from the Malá Fatra Mts.

(Spišiak & Hovorka 1997). The Cretaceous lamprophyres

from the Malá Fatra Mts. fall within the field of alkaline

lamprophyres.

For a more detailed geochemical characterization, we used

a trace element diagram normalized to primitive mantle

(Fig. 12). The contents of compatible elements (Cr, Ni, Co, V,

Sc) in the studied lamprophyres are lower (Cr, Ni) or similar to

primitive mantle (PM). This could mean that the source was

either depleted in these elements or retained by compatible

elements during partial melting. It could also indicate (espe-

cially Sc and Co concentrations) the presence of biotite and

clinopyroxene in the source. In contrast to PM, all incompa-

tible elements are highly abundant. Compared to the average

composition of calc–alkaline lamprophyres, the lamprophyres

from the Malá Fatra Mts. are rich in Nb and Ta and slightly

depleted in LILE (large-ion lithophile elements), namely Rb,

Ba and Cs. The other elements compared had identical con-

tents. Enrichment of some lamprophyre types with Nb and Ta

was also described in the Sudetes (Awdankiewicz 2007)

We also used discrimination diagrams to classify the studied

rocks with different types of magmatic formations. The Nb/Y

ratio was used as an index to ascertain the alkaline or

Fig. 6. a — Back scattered electron (BSE) images of amphiboles and

apatites, the numbers in figures correspond to those in Table 4; b —

back scattered electron (BSE) images of plagioclases, the numbers in

figures correspond to those in Table 5; Plg — plagioclases, Amp —

amphiboles, Bt — biotites, Ap — apatites.

N. anal.

SiO

39.63

40.47

39.61 SiO

35.35

35.03

35.29

TiO

5.45

4.33

5.10 TiO

3.58

5.47

5.92

11.23

10.41

11.22 Al

16.24

14.53

14.66

0.01

0.12

0.00 Cr

0.00

FeO

16.72

20.16

16.64 FeO

23.59

22.55

21.99

MnO

0.30

0.44

0.30 MnO

0.05

0.08

0.07

MgO

8.89

7.19

8.54 MgO

8.35

8.99

9.32

CaO

11.13

11.08

11.33 CaO

0.06

0.10

0.05

2.45

2.65

2.29 Na

0.14

0.09

0.11

1.42

1.55

1.51 K

9.34

9.46

9.48

1.69

1.68

1.67 H

3.90

3.89

3.92

Total

98.92 100.08

98.21 Total

100.60 100.19 100.81

6.100

6.260

6.162 Si

2.716

2.703

2.697

1.900

1.740

1.838

1.284

1.297

1.303

∑T

8.000

8.000 ∑T

4.000

0.631

0.504

0.597 Ti

0.207

0.318

0.340

0.137

0.158

0.219

0.187

0.025

0.017

0.001

0.015

0.000 Cr

0.000

2.040

1.658

1.980 Fe

1.516

1.455

1.405

0.039

0.058

0.040 Mn

0.003

0.005

2.152

2.608

2.165 Mg

0.956

1.034

1.062

∑C

5.000

□

0.131

0.162

0.171

1.835

1.836

1.888 ∑M

3.000

0.165

0.164

0.112 Ca

0.005

0.008

0.004

∑B

2.000

2.000 Na

0.021

0.013

0.016

0.567

0.631

0.579 K

0.915

0.931

0.924

0.279

0.306

0.300

□

0.059

0.047

0.055

∑A

0.845

0.937

0.879 ∑I

0.941

0.953

0.945

2.000

2.000 OH

2.000

Table 4: Selected analyses of amphiboles and biotites. Crystal-

chemical formula calculated based on 13 C+T cations (amphiboles)

and 22 negative charges (biotites).

460

SPIŠIAK, VETRÁKOVÁ, CHEW, FERENC, MIKUŠ, ŠIMONOVÁ and BAČÍK

GEOLOGICA CARPATHICA

, 2018, 69, 5, 453–466

calc–alkaline character of various rock types (Ma et al. 2013,

Jayabalan et al. 2015). The high Nb contents in the samples

would point to their alkaline character. A similar dependence

was used by Krmíček et al. (2011) for geotectonic classifica-

tion. In the discrimination diagram (Fig. 13), the examined

rocks are lying in the field of anorogenic geodynamic setting

rocks. Further, we employed the dependence of Th/Y; Ta/Yb

and Ba/Th, U/La to compare the studied lamprophyres with

main geochemical reservoirs (Fig. 14a, b). In the diagrams,

the rocks lie close to the enriched mantle field (Fig. 14a) or are

shifted toward U–Th enrichment (Fig. 14b). We also plotted

the analyses of calc–alkaline lamprophyres from the Krušné

hory Mts. (Štemprok et al. 2014).

The normalized REE curve (Fig. 15) indicates enrichment

in LREE relative to HREE, which can result from mode rate-

degrees of partial melting of the protolith. No Eu-anomaly was

observed and therefore, no accumulation or plagioclase frac-

tionation during magma evolution is likely. La/Yb ratio from

the sampled lamprophyres is consistently within 0.14 to 0.17

indicating that parental melts were probably mantle-derived

Fig. 8. Position of studied mica in the classification diagram of Abdel-

Rahman (1993) for micas from different magmatic series.

Fig. 7. Classification diagram of studied micas. End-members names

according to Rieder et al. (1998).

Sample

MH-1

DS-29

DS-55

N. anal.

1xe

4xe

SiO

59.96

55.83

52.76

60.01

54.89

52.19

52.58

53.26

53.74

53.09

53.95

64.73

65.06

TiO

0.00

0.14

0.21

0.11

0.10

0.08

0.10

0.00

25.15

27.61

29.45

25.08

28.19

29.74

28.54

28.40

29.04

28.56

18.36

18.08

FeO

0.24

0.41

0.43

0.22

0.32

0.42

0.38

0.49

0.43

0.53

0.55

0.20

0.17

MnO

0.00

0.09

0.03

0.00

0.07

0.03

0.00

0.01

CaO

6.21

9.38

11.92

6.27

9.99

12.36

12.07

12.44

12.29

12.57

11.38

0.09

0.05

MgO

0.00

0.06

0.05

0.00

0.02

0.05

0.03

0.08

0.09

0.11

0.23

0.00

BaO

0.06

0.03

0.04

0.12

0.04

0.00

0.34

0.17

SrO

0.26

0.23

0.25

0.36

0.25

0.16

0.12

0.13

0.15

0.13

0.16

0.00

7.52

5.49

4.28

7.17

5.03

4.02

4.17

3.94

4.32

3.99

4.52

0.47

0.45

0.91

0.87

0.42

0.89

0.85

0.36

0.39

0.59

0.53

0.43

0.75

15.91

16.27

Total

100.30

100.14

99.83

100.15

99.69

99.55

99.64

99.48

99.95

99.90

99.98

100.33

100.26

Formula based on 5 cations
Si

2.67

2.52

2.40

2.69

2.49

2.39

2.40

2.44

2.42

2.45

2.99

3.00

0.00

0.01

0.00

1.32

1.47

1.58

1.32

1.51

1.60

1.54

1.52

1.56

1.53

1.00

0.98

0.00

Fe3

0.00

Fe2

0.01

0.02

0.01

0.02

0.01

0.02

0.01

0.00

0.01

0.02

0.00

0.30

0.45

0.58

0.30

0.49

0.61

0.59

0.61

0.60

0.61

0.55

0.00

0.01

0.00

0.65

0.48

0.38

0.62

0.44

0.36

0.37

0.35

0.38

0.35

0.40

0.04

0.05

0.02

0.05

0.02

0.03

0.04

0.94

0.96

29.69

46.09

59.11

30.85

49.70

61.60

60.11

61.36

59.25

61.87

55.63

0.47

0.26

65.11

48.84

38.43

63.92

45.28

36.27

37.55

35.17

37.70

35.59

39.97

4.23

4.03

5.20

5.06

2.46

5.23

5.02

2.14

2.34

3.46

3.05

2.54

4.39

95.30

95.71

Table 5: Selected analyses of plagioclases and K-feldspar.

462

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, 2018, 69, 5, 453–466

Sample/ Primitive mantle

1
2
3

100

1000

0.1

0.01

Table 6: Selected analyses of apatites.

N. anal.

Figures

Fig 10c

Fig. 10d

SiO

0.13

0.14

0.15

0.10

0.09

TiO

0.00

0.08

0.09

0.05

0.00

0.03

0.00

FeO

0.55

0.47

0.54

0.51

0.53

0.58

MnO

0.11

0.20

0.14

0.16

0.12

MgO

0.10

0.11

0.14

0.17

CaO

52.79

52.51

52.85

52.81

52.27

52.70

0.14

0.11

0.13

0.09

0.10

0.01

0.00

0.02

0.01

0.00

BaO

0.07

0.05

0.01

0.00

1.53

1.36

1.49

1.41

1.53

1.63

0.35

0.36

0.35

0.34

SrO

0.10

0.09

0.12

0.10

0.00

0.01

0.00

0.02

0.01

ThO

0.02

0.03

0.00

0.01

0.02

0.00

PbO

0.04

0.00

0.02

41.14

41.43

41.69

41.36

41.48

41.47

0.08

0.02

0.08

0.04

0.03

0.02

0.13

0.18

0.13

0.17

0.10

0.11

0.33

0.40

0.33

0.36

0.26

0.25

0.01

0.07

0.01

0.10

0.00

0.16

0.15

0.14

0.16

0.15

0.13

0.02

0.00

0.03

0.06

0.01

0.00

Total

97.78

97.66

98.26

98.00

97.58

97.89

Oxygens

3.005

3.030

3.023

3.015

3.024

3.012

0.011

0.012

0.013

0.009

0.008

0.000

0.001

sum

3.016

3.042

3.036

3.028

3.034

3.021

4.880

4.861

4.850

4.872

4.823

4.845

0.000

0.003

0.000

0.005

0.006

0.003

0.039

0.034

0.039

0.037

0.038

0.041

0.008

0.014

0.010

0.012

0.008

0.013

0.012

0.013

0.014

0.018

0.021

0.023

0.018

0.022

0.016

0.017

0.001

0.000

0.003

0.001

0.000

0.002

0.000

0.005

0.004

0.006

0.005

0.000

0.001

0.000

0.001

0.000

0.001

REE+Y

0.024

0.026

0.023

0.025

0.021

0.016

sum

4.995

4.973

4.962

4.992

4.942

4.958

0.418

0.372

0.402

0.385

0.417

0.442

0.051

0.052

0.051

0.050

0.049

0.531

0.576

0.547

0.565

0.533

0.509

sum F+Cl

0.469

0.424

0.453

0.435

0.467

0.491

0.004

0.001

0.004

0.002

0.001

0.004

0.006

0.004

0.005

0.003

0.010

0.013

0.010

0.011

0.008

0.000

0.002

0.000

0.003

0.000

0.005

0.004

0.005

0.004

0.000

0.001

0.002

0.000

Total

14.511

14.450

14.485

14.418

14.453

However, the Ti enrichment in pyroxene and biotite, presence

of kaersutitic amphibole indicates an alkaline trend (Rock

1987), although similar magmatic kaersutite was reported

from calc–alkaline lamprophyres (Pivec et al. 2002). Apatite

in the studied samples has a relatively lower F content com-

pared to typical apatite from lamprophyres (e.g., Tappe et al.

2006; Seifert 2009; Pandey et al. 2018) or magmatic apatite

from granitic rocks in the Western Carpathians (Broska et al.

2004). In contrast, the Cl content in apatite is unusually high

compared to granitoids in the Western Carpathians (Broska et

al. 2004) and most of lamprophyres (e.g., Renno et al. 2003;

Tappe et al. 2006; Pandey et al. 2018). However, high Cl con-

tent in apatite is typical for post-collisional lamprophyres

(Seifert 2009).

Fig. 11. Classification diagram of lamprophyres (Rock 1987);

1 — studied lamprophyres, 2 — calc–alkaline lamprophyres, 3 — ave-

rage spessartite (data for calc–alkaline lamprophyres and spessartite

from Rock (1991), 4 — Cretaceous alkaline lamprophyres from Malá

Fatra Mts. (Hovorka & Spišiak 1988).

Fig. 12. Trace element concentrations normalized to the composition

of the primordial mantle (McDonough & Sun 1995); 1— studied

lamprophyres, 2 — calc–alkaline lamprophyres, 3 — average spessar-

tite (data for calc–alkaline lamprophyres and spessartite from Rock

(1991).

464

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, 2018, 69, 5, 453–466

both types of rocks are very similar in composition. Regarding

the fact they are xenocrysts, we suppose that they grew in

the basic melt at great depth, at the site of its generation.

The same age of rocks, the same type of xenocrysts and

the same type of their alteration point to possible comagmatic

origin of Permian paleobasalts (melaphyres) in the Hronicum

and Late Paleozoic calc–alkaline lamprophyres from the Malá

Fatra Mountains.

The age of the studied rocks has not been precisely deter-

mined yet and it is thus estimated according to their geological

position. The lamprophyre dykes cut the Variscan medium-

grained granodiorities to tonalities, but do not penetrate

the cover Mesozoic complexes. The age of the surrounding

granites was determined by Scherbak et al. (1990) at 353 Ma.

In general, the age of lamprophyre is estimated to Late

Paleozoic. The determined age of the rocks using LA-ICP-MS

by apatite analysis of 263.4 ± 2.6 Ma corresponds to their geo-

logical position.

Conclusions

The lamprophyric dyke rocks in the Malá Fatra core moun-

tain which intruded the Variscan granites are strongly altered.

Xenoliths of the surrounding granite rocks and minerals

(especially plagioclase) are frequently observed and they are

resorbed to different degrees.

Clinopyroxene, amphibole, biotite, plagioclase and potas-

sium feldspar are preserved as primary minerals. Clinopyroxene

occurs as phenocrysts, but rarely also as xenocrysts. These two

types of clinopyroxene are different in chemical composition.

Amphibole (kaersutitic) and biotite are characteristic for high

TiO

content.

Based on the main and rare element content, they corre-

spond to calc–alkaline lamprophyres with an affinity to alka-

line lamprophyres.

Variations in the chemical composition of lamprophyres

(including Sr and Nd isotopic compositions) are probably

the result of the primary mantle magma contamination by

crustal materials.

The LA-ICP-MS U–Pb age for apatite from Malá Fatra

Mts. lamprophyres is 263.4 ± 2.6 Ma. The age is similar to

the calc–alkaline lamprophyres from the Nízke Tatry Mts.

Acknowledgements: This research was supported by grants

VEGA 1/0650/15, 1/0237/18 and APVV 15-0050. We appre-

ciate the critical reviews by handling editors Pavel Uher and

Igor Broska, an anonymous reviewer, and Jaromír Ulrych,

who helped to improve the manuscript.

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