ORIGINAL PAPER

Dioritic intrusions of the Slavkovsky les (Kaiserwald),Western Bohemia: their origin and significance in lateVariscan granitoid magmatism

Pavla Kovarıkova Æ Wolfgang Siebel ÆEmil Jelınek Æ Miroslav Stemprok Æ Vaclav Kachlık ÆFrantisek V. Holub Æ Vratislav Blecha

Received: 15 October 2007 / Accepted: 15 December 2008 / Published online: 8 January 2009

� Springer-Verlag 2008

Abstract Mafic and intermediate intrusions occur in the

Slavkovsky les as dykes, sills and minor tabular bodies

emplaced in metamorphic rocks or enclosed in late Variscan

granites near the SW contact of the Western Krusne hory/

Erzgebirge granite pluton. They are similar in composition

and textures to the redwitzites defined in NE Bavaria. Single

zircon Pb-evaporation analyses constrain the age of a quartz

monzodiorite at 323.4 ± 4.4 Ma and of a granodiorite at

326.1 ± 5.6 Ma. The P–T range of magma crystallization

is estimated at *1.4–2.2 kbar and *730–870�C and it

accords with a shallow intrusion level of late Variscan

granites but provides lower crystallization temperatures

compared to the Bavarian redwitzites. We explain the het-

erogeneous composition of dioritic intrusions in the

Slavkovsky les by mixing between mafic and felsic magmas

with a minor effect of fractional crystallization. Increased

K, Ba, Rb, Sr and REE contents compared to tholeiitic

basalts suggest that the parental mafic magma was probably

produced by melting of a metasomatised mantle, the melts

being close to lamprophyre or alkali basalt composition.

Diorites and granodiorites originated from mixed magmas

derived by addition of about 25–35 and 50 vol.%, respec-

tively, of the acid end-member (granite) to lamprophyre or

alkali-basalt magma. Our data stress an important role of

mafic magmas in the origin of late Variscan granitoids in

NW Bohemian Massif and emphasize the effect of mantle

metasomatism on the origin of K-rich mafic igneous rocks.

Keywords Diorite � Redwitzite � Slavkovsky les �Variscan magmatism � Zircon dating �Gravity measurements � Magma mixing

Introduction

Redwitzites were originally defined in the NW part of the

Bohemian Massif in NE Bavaria (Willmann 1920), and

comprise mafic to intermediate Variscan igneous rocks

ranging from diorites to quartz monzonites. They are

characterised by large biotite crystals enclosing plagioclase

grains in coarse- to medium-grained textures. Their min-

eralogy, geochemistry and isotopic composition in Bavaria

was studied by Troll (1968), Miessler and Propach (1987),

Spiegel and Propach (1991), Holl et al. (1989), Siebel

(1994), Siebel et al. (1995, 2003) and Freiberger et al.

(2001), while rocks similar to redwitzites were reported in

Bohemia by Rene (2000) and Kovarıkova et al. (2007).

Redwitzites are characterized by variable compositions

over short distances, and this feature has been interpreted

as reflecting variable degrees of mixing between mafic and

felsic magmas (e.g. Holl et al. 1989). Geochronological

measurements show that dioritic rocks in NW Bohemia and

redwitzites in the northern Oberpfalz were formed at about

325 Ma (Siebel et al. 2003, Kovarıkova et al. 2005) coeval

with the emplacement of late Variscan granites of the

Krusne hory/Erzgebirge batholith (Kempe et al. 2004;

Romer et al. 2007). Fiala (1968) noticed a compositional

similarity between mafic intrusions in the Slavkovsky les

P. Kovarıkova � E. Jelınek � M. Stemprok � V. Kachlık �F. V. Holub � V. Blecha

Faculty of Science, Charles University in Prague,

Albertov 6, 128 43 Prague 2, Czech Republic

W. Siebel

Universitat Tubingen, Wilhelmstr. 56,

720 74 Tubingen, Germany

P. Kovarıkova (&)

Czech Geological Survey, Geologicka 6,

152 00 Prague 5 - Barrandov, Czech Republic

e-mail: graptolit@seznam.cz; pavla.kovarikova@geology.cz

123

Int J Earth Sci (Geol Rundsch) (2010) 99:545–565

DOI 10.1007/s00531-008-0406-0

and redwitzites in NE Bavaria, but he used the name

‘‘redwitzite’’ only for the mafic rocks with a planar texture.

In our recent paper (Kovarıkova et al. 2007) we employed

the term ‘‘redwitzite’’ for the Krusne hory/Erzgebirge

‘‘gabbrodioritic’’ and ‘‘gabbronoritic’’ rocks to stress their

genetic connection with the mafic and intermediate rocks in

NE Bavaria. Although many late Variscan mafic and

intermediate bodies in the Saxothuringian Zone of the

Central European Variscides are probably of a similar

genesis, many petrologists prefer the use of the term

‘‘redwitzite’’ in their original localities in NE Bavaria.

Thus, in the present paper, we employ the term ‘‘dioritic

rocks’’ to refer to a wide compositional range of spatially

scattered intrusions in which the dioritic compositions

prevail.

Data from new gravity and magnetic surveys determined

the form of a large mafic body within the metasediments of

the Slavkovsky les, the measurement being enabled by the

distinct contrast in densities and magnetic properties from

hosting metasediments. Based on our new data, we revisit

the role of mafic magmatism in the genesis of granitoids in

the Slavkovsky les and discuss it more broadly in relation

to late Variscan granitoid magmatism in Western Bohemia

where a number of authors have stressed the role of mafic

magmas in granite petrogenesis (Siebel et al. 1997;

Trzebski et al. 1997).

Geological setting

The Slavkovsky les (Kaiserwald) in western Bohemia is a

geomorphologically constrained hilly area reaching heights

of about 800 m a.s.l. within the triangle of the towns

Karlovy Vary, Marianske Lazne and Frantiskovy Lazne

(Fig. 1). The granitoids of the Slavkovsky les intrude the

Slavkovsky les Crystalline Unit (SLCU), which is over-

lained by allochtonous Kladska Unit and Marianske Lazne

Complex (MLC, Kachlık 1993, 1997; Fig. 2). The SLCU is

composed of variably metamorphosed mica schists,

gneisses and migmatites, locally reaching the sillimanite

facies of regional metamorphism. The Kladska Unit is a

tectonic slice composed of weakly metamorphosed LP-LT-

MT banded schists with intercalations of graphitic schists

and quartzites accompanied by the products of bimodal

volcanism (Kachlık 1997). The overlying MLC is a tec-

tonic stack of several mafic HP and MP units of

metaophiolitic origin derived from the Saxothuringian

ocean (Franke 1989).

30 km

Marktredwitz

Erbendorf

Cheb

DCZ

Bh

Md

LgSx

Ms

Bohemian Massif

mafic to ultramafic metamorfic rocks(with associated metasediments)

Variscan granitoids

Tertiary sediments

basement crystalline units

fault

Prague

Františkovy

Kirchberg massif

Nejdek - Eibenstock massif

Bergen massif

Karlovy Vary massif

Bor massif

Cheb basin

Sokolov basin

Abertamy mafic body

Tertiary volcanics

dioritic intrusions and redwitzites

Pre-Variscan granites

Carboniferous-Permian sediments

area in Fig. 2

massif

North Oberpfalz massif

town

Karlovy Vary

Fig. 1 Geological map of redwitzites and dioritic rocks (redrawn

using the geological map 1:500,000 of the Czech Geological Survey

(Chab et al. 2007) and the data from Siebel (1993) and Rene (2000).

The location of the study area is indicated by a quadrangle. Overview

map (upper right) shows tectonostratigraphical units of the Bohemian

Massif: Sx Saxothuringian, Lg Lugian, Bh Bohemian, Md Moldan-

ubian, Ms Moravo-Silesian (Mısar et al. 1983)

546 Int J Earth Sci (Geol Rundsch) (2010) 99:545–565

123

The granitoids in the Western Krusne hory/Erzgebirge,

Vogtland and the Slavkovsky les outcrop in two major

granitic massifs, the northern one called the Nejdek-

Eibenstock massif north of the Ohre (Eger) rift zone, and

the Karlovy Vary massif to the south and south-east, the

latter extending from Karlovy Vary to the vicinity of

Marianske Lazne (Fig. 1). The granitoids of the Slavkovsky

les are part of the Karlovy Vary massif, which together with

Nejdek-Eibenstock massif forms a single tabular body

about 10 km thick (Tomek et al. 1994) as based on the

seismic data. The granitic sequence consists of a number of

intrusive phases that form two compositionally distinct

suites (Older and Younger Intrusive Complexes, OIC, YIC,

respectively, Lange et al. 1972, Stemprok 1986), each

traditionally differentiated within the southern part of the

Nejdek-Eibenstock massif as ‘‘Gebirgsgranite’’ and

‘‘Erzgebirgsgranite’’ (Laube 1876). The OIC granites are

mainly low-fluorine and low Li biotite monzogranites

(Forster et al. 1999), while YIC granites are high-fluorine

lithium-mica syenogranites and alkali feldspar granites.

Transitional granites (TR), defined for the first time by Fiala

(1968) in the Slavkovsky les, comprise mainly two-mica

granites with moderately high Li and F contents.

The predominant granite type in the northeastern and

eastern part of the Slavkovsky les is porphyritic biotite

granite (OIC), which is crosscut by aplites and aplitic

granites (Kratochvıl 1959). The YIC granites crop out as

two composite intrusions (Krudum and Lesny-Lysina,

Fig. 2). The contact of the OIC and YIC granites with the

metamorphic envelope is sharp and intrusive. Scarce

enclaves of dioritic composition are found in OIC granites

while YIC granites are practically barren of them. The

eastern contact of the Krudum massif dips flatly to the east

as documented by numerous drill holes carried out for

exploration of tin ores in the vicinity of Hornı Slavkov

(Najman et al. 1988). TR granites occur in the northern part

of the Slavkovsky les in association with the OIC granites,

and in the Lesny-Lysina massif in contact with YIC

granites (Fig. 2).

OIC granite in the southern part of the Nejdek-Eiben-

stock massif yielded an age of 322 Ma (Kovarıkova et al.

2007). The YIC granites have zircon ages between 323 and

318 Ma (Forster et al. 1999; Kempe et al. 2004; Romer

et al. 2007) as documented in the northern part of the

intrusion. Dioritic intrusions in the southern Nejdek-

Eibenstock massif and redwitzites in NE Bavaria show

zircon ages between 325 and 323 Ma (Taubald 2000;

Siebel et al. 2003; Kovarıkova et al. 2007) and belong thus

to the first cycle of Variscan granitoid magmatism in the

Krusne hory/Erzgebirge (Siebel et al. 1997).

Both steep (roadcut NW of Becov) and flat contacts (the

Uhlırsky vrch) between dioritic intrusions and metamor-

phic host rocks have been observed. The presence of blocks

of host garnet amphibolites (up to several metres) in the

granodiorite in the roadcut profile NW of Becov suggests a

role for active stopping. Some dioritic intrusions show

chilled margins, characterized by the absence of large

biotite crystals and a decrease in grain size of the matrix

Fig. 2 Geological map of

granitoid plutons and crystalline

units in the Slavkovsky les and

vicinal areas (according to the

geological maps 1:200,000

(Zoubek 1963) and 1:50,000

(Schovanek et al. 2001) Czech

Geological Survey). OIC‘‘Older Igneous Complex’’, YIC‘‘Younger Igneous Complex’’,

TR transitional granites, msmuscovite, bi biotite

Int J Earth Sci (Geol Rundsch) (2010) 99:545–565 547

123

minerals at the contact with metamorphic host rocks. The

surrounding metasediments are transformed into biotite or

amphibole-biotite hornfelses with granoblastic textures.

The relationships of quartz diorite/quartz monzodiorite

with the OIC granite could not be determined because of

the lack of joint outcrops. A subvertical contact between

OIC porphyritic biotite granite and amphibole biotite

granodiorite has been documented in the roadcut NW of

Becov. The porphyritic biotite granite has a strong plano-

linear fabric close to the contact, with ductile deformation

of biotite and feldpar phenocrysts. The contact between

quartz monzodiorites and YIC granites is exposed in the

Vıtkov quarry in the NE margin of the Krudum massif.

Fine-grained porphyritic quartz monzodiorites, forming

several tens of meters large and several meters thick,

mostly flat lying plate-like bodies, are separated by a sharp

contact from the fine to medium-grained YIC granite.

Quartz monzodiorites and YIC granites are intersected by

later aplites.

Dioritic intrusions were petrographically studied by

Kratochvıl (1959) and Fiala (1961a, 1968) in the course of

geological mapping of the Slavkovsky les on scale 1:5,000.

They were named as ‘‘gabbrodiorite’’ (NE of Lazne

Kynzvart and at the Uhlırsky vrch), diorite (quarry Vıtkov),

quartz diorite (SW of Hornı Slavkov) and granodiorite (near

Becov) (Fig. 3). In this study we apply IUGS nomenclature

(LeMaitre et al. 1989), shown in the QAP diagram (Fig. 4),

which disregards the term ‘‘gabbrodiorite’’.

Mine workings and drill holes east of the Krudum

massif (Stemprok 1971) show that most dioritic intrusions

are tabular or lens-like bodies (sills). Some of them have

apparent gradual contacts with the metamorphic envelope

whereas others appear to be separated by sharp contacts

mainly from enclosing paragneisses. Many dioritic rocks

are associated with thin aplitic dykes, small pegmatitic

lenses or are interlayered with paragneisses.

Sampling and analytical techniques

Samples (each between 5 and 15 kg) were taken from

outcrops (quartz monzodiorite Lo2, Lo3, Vı1, quartz dio-

rite Lo4 and granodiorite Hr1, Be1, Be2 and Be3) or large

boulders (gabbronorite Lo1). About half of each sample

was crushed and gradually split into smaller volume and

the amount of about 50–100 g was pulverized in an agate

mortar for chemical analyses. Major and trace element

analyses on selected whole-rock samples were made in the

laboratories of the Geological Institute at the Faculty of

Science, Charles University, Prague by wet chemical

methods (major elements), inductively coupled plasma

mass spectrometry (ICP-MS) (REE and trace elements) and

Fig. 3 Geological map of the Hornı Slavkov—Krasno area simplified

from the 1:50,000 geological map, sheet Sokolov, Czech Geological

Survey (Schovanek et al. 2001). Variscan granite groups: OIC ‘‘Older

Igneous Complex’’, YIC ‘‘Younger Igneous Complex’’, TR transi-

tional granites, MLC Marianske Lazne Complex, Mineral

abbreviations: bi biotite, ms muscovite, sil sillimanite. Sampling

localities: UV Uhlırsky vrch, 1 quartz monzodiorite and quartz diorite

at the Uhlırsky vrch, 2 quartz monzodiorite at quarry Vıtkov, 3 quartz

monzodiorite in the Lobzy brook valley, 4 quartz diorite near Hornı

Slavkov, 5 granodiorite near Becov

548 Int J Earth Sci (Geol Rundsch) (2010) 99:545–565

123

atomic absorption spectrometry (AAS) (Ba, Be, Cs, Co, Cr,

Ni, Pb, Rb, Sr, V and Zn). Analyses of fluorine were made

in the Central Laboratories of the Czech Geological Survey

in Prague. The accuracy for major oxides and F determi-

nation is \1.5% and for trace elements determined by

AAS \ 1%. The maximum deviations for ICP-MS analy-

ses are 5% for trace elements and 3% for REE. Earlier

literature major oxides analyses (Fiala 1968) have slightly

lower accuracies of about 2–3%.

Selected samples were analysed by electron microprobe

(CAMECA SX-100) at the Institute of Geology, Academy

of Science, Prague, in wavelength dispersive mode.

Plagioclase compositions determined by electron micro-

analyzer were supplemented by optical studies on a larger

set of samples. Heavy mineral fractions were prepared in

the laboratories of the Czech Geological Survey. The

crushed samples were separated using heavy liquids and

zircons were handpicked from the heavy mineral assem-

blage after magnetic separation.

For single-zircon Pb-evaporation (Kober 1986, 1987)

chemically untreated zircon grains were analysed with a

Finnigan MAT 262 mass spectrometer equipped with a

secondary electron multiplier (SEV) at the University of

Tubingen. Measured 207Pb/206Pb ratios were corrected for

common Pb according to the formula given in Cocherie

et al. (1992) following the Pb evolution model of Stacey

and Kramers (1975). No correction was made for mass

fractionation. The common Pb corrected 207Pb/206Pb ratios

normally have a Gaussian distribution and the mean of

the 207Pb/206Pb ratios was derived from this distribution.

The error for a single zircon age was calculated according

to the formula

Dage ¼

ffiffiffiffiffiffiffiffiffiffiffiffiffiffiffiffiffiffiffiffiffiffiffiffiffiffiffi

2rffiffiffi

np� �2

þDf 2

s

:

where n is the number of 207Pb/206Pb isotope ratio scans,

2r is the 2sigma standard deviation of the 207Pb/206Pb

ratios derived from the Gaussian distribution function and

Df an assumed error for the measured 207Pb/206Pb ratios of

0.1% which includes potential bias caused by mass frac-

tionation of Pb isotopes and uncertainty in linearity of the

multiplier signal. The mean zircon age for samples Lo2

(quartz monzodiorite) and Be3 (granodiorite) is given as

Q

monzo−granite

grano−diorite

tonalite

quartz−monzonite

q−monzodiorite q−monzogabbro

q−dioriteq−gabbroq−anorthosite

monzonite

monzodioritemonzogabbro

diorite, gabbro

A P

Fig. 4 QAP diagram of dioritic intrusions in the Slavkovsky les

based on modal analyses

Fig. 5 Microphotographs

illustrating the textures of

dioritic intrusions: a fine-

grained texture of quartz

monzodiorite from the mafic

body at the Uhlırsky vrch;

b pressure induced bending of

plagioclase crystals (quartz

monzodiorite); c inclusion of

biotite in plagioclase

(granodiorite). Mineral

abbreviations: bi biotite,

plg plagioclase

Int J Earth Sci (Geol Rundsch) (2010) 99:545–565 549

123

weighted average and the error refers to the 95% con-

fidence level (ISOPLOT, Ludwig 1999). Repeated

measurements on two internal standard zircons of similar

age as most of the studied samples were performed for

geologically realistic age and error treatment.

For calculation of temperatures and pressures from

mineral pairs and from saturation temperatures the

Newamphcal (Yavuz 1999) and GCDkit (Janousek et al.

2006) were employed. Fractional crystallization was

modelled using the program FC-Modeler (Keskin 2002).

Petrography

Quartz monzodiorite

Quartz monzodiorite bodies are confined to the northern

exocontact of the Krudum granite massif (Fig. 3). The

largest outcrop (ca. 600 9 350 m) occurs at the hill 720 m

a.s.l. (called the Uhlırsky vrch, locality 1 in Fig. 3). The

rock type occurs at the contact with the YIC Li-mica

granite, minor intrusion of OIC granite and the metamor-

phic envelope of cordierite-sillimanite hornfelses and

hornfelsic or migmatized paragneisses (Fiala 1961b).

Medium-grained quartz monzodiorite (1–2 mm grain size)

builds up the central part of the intrusion while fine-grained

variety (about 0.5 mm) occurs at the margin. The texture

is mostly hypidiomorphic-granular, randomly oriented

(Fig. 5a). In some marginal parts quartz monzodiorite

irregularly passes into quartz diorite.

The rock contains large flakes of biotite (*30 vol.%,

Table 1), commonly chloritised along rims typical of the

medium-grained variety. Biotites as oikocrysts frequently

enclose amphibole and plagioclase crystals. Plagioclase

An14–An48 (30–35 vol.%) (Fig. 6) is mostly unzoned and

occasionally deformed (Fig. 5b), some plagioclase crys-

tals have irregular cores of more basic composition

(An68–80). Zoned plagioclase is predominantly andesine

(An40–44), rarely some zones range about An60. Almost

colourless to light yellow–green amphiboles of horn-

blende to actinolite composition (21–24 vol.%, Table 2)

form individual crystals or dense aggregates. Secondary

amphiboles (actinolite) commonly form pseudomorphs

after clinopyroxenes or primary magmatic amphiboles.

Relicts of diopsidic pyroxene (5 vol. %, Table 3) were

observed in intergrowths with amphiboles. Allotriomor-

phic alkali feldspar crystals (orthoclase; up to 5 vol.%)

are associated with rare quartz and Na-plagioclase

(An14). Accessory minerals are apatite (strongly pig-

mented and in places pleochroic), zircon and, in lesser

amount ilmenite, titanite, allanite, rutile, magnetite and

pyrrhotite. In some biotite flakes prehnite occurs along

the cleavage.

Table 1 Representative electron microprobe analyses of biotite from

quartz monzodiorite (Lo2, Vı1) and granodiorite (Be3)

Sample Vı1 Vı1 Lo2 Lo2 Be3 Be3

SiO2 36.46 37.11 36.52 36.15 36.64 35.88

TiO2 3.47 3.46 3.62 3.74 4.00 4.10

Al2O3 14.20 14.27 14.76 14.64 14.65 14.83

FeO 17.30 16.83 18.28 18.45 18.17 19.23

MnO 0.26 0.08 0.24 0.24 0.31 0.25

MgO 12.29 12.96 11.50 11.60 10.93 10.54

CaO 0.03 0.02 0.06 0.02 0.03 0.05

Na2O 0.13 0.13 0.11 0.12 0.17 0.09

K2O 9.50 9.63 9.44 9.49 9.62 9.24

Total 93.64 94.49 94.53 94.45 94.52 94.21

Number of ions calculated to 22 (O)

Si 5.630 5.654 5.603 5.565 5.626 5.552

AlIV 2.370 2.346 2.397 2.435 2.374 2.448P

(T) 8.000 8.000 8.000 8.000 8.000 8.000

AlVI 0.214 0.216 0.271 0.220 0.277 0.256

Ti 0.403 0.396 0.418 0.433 0.462 0.477

Mg 2.829 2.944 2.630 2.662 2.502 2.431

Fe 2.234 2.144 2.345 2.375 2.333 2.488

Mn 0.034 0.010 0.031 0.031 0.040 0.033P

(M) 5.715 5.710 5.695 5.722 5.614 5.685

Ca 0.005 0.003 0.010 0.003 0.005 0.008

Na 0.039 0.038 0.033 0.036 0.051 0.027

K 1.871 1.871 1.847 1.863 1.884 1.824P

(I) 1.915 1.913 1.890 1.902 1.940 1.859

mg 55.88 57.86 52.86 52.85 51.75 49.42

Oxides in wt.%. mg = 100 Mg/(Mg ? Fetotal)

Fig. 6 Electron microprobe analyses of felspars from dioritic

intrusions

550 Int J Earth Sci (Geol Rundsch) (2010) 99:545–565

123

Small bodies of fine-grained quartz monzodiorite rang-

ing in sizes from several metres to tens of metres were

studied in the quarry at Vıtkov (NW of Uhlırsky vrch,

locality 2 in Fig. 3), where YIC granites surround them.

Quartz diorite

Minor outcrops of fine-grained quartz diorite of

*0.3–0.5 mm grain size occur in the Lobzy brook valley

(Fig. 3, locality 3). Amphibole (hornblende, 15–20 vol.%)

predominates over biotite (*10 vol.%), which encloses

mainly apatite (commonly zoned) and zircon crystals. Other

accessories are titanite, allanite and pyrrhotite. Oikocrysts

of biotite reach up to 1 mm in size. K-feldspar (8–12 vol.%)

forms phenocrysts commonly overgrown by plagioclase

and amphibole (Table 2). Plagioclases An35–An40 (*50%)

are weakly zoned and sporadically twinned and quartz

(c. 8 vol.%) fills the interstices. Clinopyroxene (c. 3 vol.%)

of diopsidic composition is intergrown with or partly

replaced by green amphibole while the amphibole aggre-

gates are commonly overgrown by biotite.

Similar quartz diorites were found during uranium

mining in underground workings and boreholes in the

surrounding of Hornı Slavkov and Krasno (Stemprok 1959,

Janecka et al. 1973; Najman et al. 1988) (Fig. 3, locality 4).

The diorite bodies with biotite as the predominant mafic

mineral were encountered near the upper contact of the

YIC granites and between paragneisses and migmatised

paragneisses (Figs. 7, 8). No diorites were found in the

underlying YIC granites in any of the mine workings and

drill holes. The boreholes south of Hornı Slavkov (K-12,

K-18, K-20, K-23, K-25; Fig. 7) encountered a number of

discontinuous diorite sills in the crystalline at depths

between 60 and 140 m, up to 300 m wide. In zones

Table 2 Representative electron microprobe analyses of amphiboles from quartz monzodiorite (Lo2, Vı1) and granodiorite (Be3)

Sample Vı1 Vı1 Vı1 Be3 Be3 Lo2 Lo2 Lo2

Type hb hb hb hb act hb act act

SiO2 51.46 49.62 44.44 50.67 51.88 47.58 54.88 54.65

TiO2 0.59 0.80 1.21 0.74 0.50 1.04 0.09 0.11

Al2O3 4.16 5.80 10.24 4.73 3.84 6.90 1.08 1.22

FeO 12.76 13.26 16.76 13.54 13.54 14.65 13.01 13.19

MnO 0.31 0.33 0.37 0.38 0.49 0.04 0.06 0.43

MgO 14.86 13.94 9.99 13.62 14.09 12.18 15.23 15.11

CaO 11.98 11.80 11.87 11.77 11.81 12.08 12.51 12.33

Na2O 0.63 0.83 1.11 0.58 0.61 0.74 0.13 0.11

K2O 0.35 0.51 1.24 0.44 0.31 0.66 0.06 0.05

Total 97.10 96.89 97.23 96.47 97.37 96.87 97.04 97.20

Number of ions calculated to 23 (O)

Si 7.442 7.231 6.668 7.422 7.534 7.115 7.938 7.886

Al 0.558 0.769 1.332 0.578 0.466 0.885 0.062 0.114P

(T) 8.000 8.000 8.000 8.000 8.000 8.000 8.000 8.000

Al 0.151 0.227 0.479 0.239 0.191 0.331 0.122 0.093

Ti 0.064 0.088 0.137 0.082 0.055 0.117 0.010 0.012

Mg 3.204 3.029 2.235 2.974 3.050 2.715 3.284 3.251

Fe (III) 0.325 0.352 0.203 0.235 0.263 0.109 0.000 0.144

Fe (II) 1.218 1.263 1.899 1.423 1.381 1.722 1.574 1.447

Mn 0.038 0.041 0.047 0.047 0.060 0.005 0.007 0.053P

(C) 5.000 5.000 5.000 5.000 5.000 5.000 5.000 5.000

Ca 1.856 1.842 1.908 1.847 1.837 1.935 1.939 1.906

Na 0.144 0.158 0.092 0.153 0.163 0.065 0.036 0.031P

(B) 2.000 2.000 2.000 2.000 2.000 2.000 2.000 2.000

Na 0.033 0.077 0.231 0.012 0.009 0.150 0.000 0.000

K 0.065 0.095 0.237 0.082 0.057 0.126 0.011 0.009P

(A) 0.097 0.172 0.468 0.094 0.066 0.276 0.011 0.009

mg 67.50 65.22 51.53 64.21 64.97 59.72 67.60 67.14

Oxides in wt.%. mg = 100 Mg/(Mg ? Fetotal)

hb magnesiohornblende, act actinolite

Int J Earth Sci (Geol Rundsch) (2010) 99:545–565 551

123

characterized by interlayering with the country rock, they

constitute swarms reaching the total thickness of 80 m

(Fig. 8). Diorites are often associated with pegmatites

(feldspar, quartz ± biotite), aplites or tonalites (Fiala

1968) and enclose intercalated paragneisses.

Gabbronorite

A single sample (Lo4) texturally very similar to gabbro-

norite from Abertamy (Kovarıkova et al. 2007) was found

in the Lobzy brook valley in spatial association with quartz

diorite. We interpret its position as a gabbroic cumulate in

dioritic rocks. It is composed of totally uralitized short

columnar crystals (19–23 vol.%) most probably after

orthopyroxene as shown by the crystal outline. Poikilitic

non-zonal plagioclase crystals An76–78 (*20 vol.%) reach

0.8 mm in size. Green amphibole (hornblende, c. 28 vol.%)

replaces or is intergrown with minor clinopyroxene. Large

oikocrysts of brown biotite, up to 1 mm in size (*24

vol.%), enclose apatite crystals (commonly zoned). Quartz

and K-feldspar crystals are very rare. Other accessories are

zircon, titanite, allanite and pyrrhotite. The petrographic

identification based on the texture is supported by the

whole rock geochemistry (see below).

Granodiorite

An elongated body (with a major axis of about 800 m) and

several small vicinal bodies of medium-grained granodio-

rite (*1–2 mm grain size) occur north and northeast of

Becov (Fig. 3, locality 5) in porphyritic biotite monzo-

granite (OIC). The granodiorite has a massive texture and

passes locally into quartz diorite. Plagioclase (An29–An52)

(35–50 vol.%) prevails over K-feldspar (up to 20 vol.%).

Tabular plagioclase normally shows weak zoning with

more sodic margins (andesine) and more calcic cores (acid

labradorite). Some plagioclase crystals are irregularly

zoned and andesine is unevenly replaced by oligoclase

domains. Quartz (c. 18 vol.%), with undulatory extinction,

commonly fills intergranular spaces. Green amphibole

(Mg-hornblende and actinolite; 4 vol.%), is partly replaced

by biotite. Biotite (10–15 vol.%) often contains inclusions

of apatite, zircon and allanite. Other accessory minerals are

titanite and tourmaline. Many large biotite flakes enclose

plagioclase crystals, however, small tiny crystals of biotite

were also observed to be enclosed in larger plagioclase

grains (Fig. 5c).

Geophysical measurements

The extent of the largest mafic body at the Uhlırsky vrch

was surveyed by gravity and magnetic methods. It was

expected that magnetometry would indicate its near-sur-

face distribution, while gravity would show the depth

extent.

Two geophysical profiles were staked out across the

quartz monzodiorite body at the Uhlırsky vrch. Figure 9

shows their location with respect to geology. The distance

between the gravity stations on the profiles was 50 m; the

distance between magnetic stations was 10 m. Results of

the geophysical measurements are shown in Fig. 10. The

dioritic intrusion on the summit of the Uhlırsky vrch pro-

duces higher and more variable magnetic field values in the

central parts of both profiles. According to field measure-

ments, the magnetic susceptibility of the mafic body is

approximately two orders of magnitude higher than that of

surrounding rocks (Blecha et al. 2004). On both ends of the

profiles, the magnetic field is relatively quiet with generally

higher values on profile 1. This indicates that the dioritic

rocks are closer to the surface in the E–W direction than in

N–S direction. Rapidly decreasing gravity values (Bouguer

anomalies) on the eastern side of profile 1 and on the

Table 3 Electron microprobe analyses of pyroxenes from quartz

monzodiorite (Lo2)

Sample Lo2 Lo2 Lo2 Lo2

Type dps dps dps dps

SiO2 52.99 53.36 52.45 53.06

TiO2 0.03 0.03 0.06 0.10

Al2O3 0.21 0.22 0.35 0.71

FeO 10.13 9.22 9.62 9.86

MnO 0.47 0.50 0.42 0.49

MgO 12.26 12.43 12.35 12.54

CaO 23.18 24.04 23.82 23.36

Na2O 0.07 0.0 0.10 0.31

K2O 0.00 0.03 0.02 0.01

Total 99.34 99.83 99.19 100.44

Number of ions calculated to 6 (O)

Si 2.000 2.000 1.991 1.987

Al 0.000 0.000 0.009 0.013P

(T) 2.000 2.000 2.000 2.000

Al 0.015 0.016 0.007 0.018

Ti 0.001 0.001 0.002 0.003

Mg 0.692 0.696 0.699 0.700

Fe 0.321 0.291 0.305 0.308

Mn 0.015 0.016 0.014 0.016

Ca 0.940 0.968 0.969 0.937

Na 0.005 0.000 0.008 0.022

K 0.000 0.001 0.001 0.000

Total 1.992 1.990 2.004 2.005

mg 68.31 70.52 69.62 69.44

Oxides in wt.%. mg = 100 Mg/(Mg ? Fetotal)

dps diopside

552 Int J Earth Sci (Geol Rundsch) (2010) 99:545–565

123

northern side of profile 2 indicate that the mafic intrusion

ends or thins out towards the east and north.

In order to assess the thickness and size of the mafic

rock body 2.75-dimensional models along both profiles

(Fig. 10) were constructed to compute the theoretical

gravity response. Constraints of the model were gravity and

magnetic measurements, the geological situation and the

densities of rocks (taken from Polansky et al. 1973). The

attempt to use the density of the Abertamy gabbronorite

(2850 kg/m3, Kovarıkova et al. 2007) gave no reasonable

geological solution for the geophysical modelling. The

results were improved when a lower density (2,760 kg/m3)

was used, which suggests a less mafic composition for the

whole body including its uncovered parts. However, a

smaller density can be also caused by interlayered para-

gneiss (2,670 kg/m3) as found in some drill holes near

Krasno.

We conclude that the dioritic intrusion at the Uhlırsky

vrch is a plate-like body about 400 m thick striking NE and

dipping NW. At depth this body is probably interconnected

with vicinal mafic rocks outcropping in the valley

approximately 1 km SW (Fig. 9). Thus the whole mafic

body can be 2 km in its longest dimension.

Geochemistry

Major oxides

The SiO2 contents in dioritic rocks fluctuate over a wide

range, from 51 wt.% (quartz diorite), between 53 and

57 wt.% (quartz monzodiorite) and between 59 and

61 wt.% for granodiorite (Table 4). The gabbronorite

contains 52.5 wt.% of SiO2. Thus the samples cover the

silica range of mafic and intermediate igneous rocks. The

TiO2 contents range between 0.6 and 1.5 wt.% and are

lower than some values reported by Fiala (1968) for dior-

ites (about 2.5 wt.% TiO2). MgO contents vary from 3.7 to

9.0 wt.% with the highest value in gabbronorite. The mg

number [100 Mg/(Mg ? Fetotal)] is about 60 for all studied

rock types. Potassium contents are relatively high

(2.7–3.5 wt.% K2O for dioritic rocks and 1.5 wt.% for

gabbronorite) showing that the rocks belong to high-K or

shoshonitic magmas (Rollinson 1993). Na2O contents vary

from 1.1 to 3.2 wt.% and K2O/Na2O ratios range from 0.8

to 1.4. The P2O5 contents are generally low (0.2–0.6 wt.%)

and differ from the values reported by Fiala (1968), which

show P2O5 contents close to 1 wt.% (Fig. 11).

Fig. 7 Underground surface of a Li-mica granite body in the Krasno area (according to Just in Janecka et al. 1973). Black circles show the drill

holes that reach diorite intrusions. Grey fields indicate probable subsurface extent of single diorite dykes or swarms

Int J Earth Sci (Geol Rundsch) (2010) 99:545–565 553

123

200 m

100 m

0 mK-25 K-23 K-20 K-12 K-18

alluvium

aplite

Li-mica albite granite

bi-amp diorite

paragneiss

migmatite andmigmatized gneiss

drill hole drill hole drill hole drill hole drill holeFig. 8 Geological profiles of

five drill holes from the Krasno

ore district in the crystalline

complex of the Central

Slavkovsky les showing the

position of diorite bodies above

the YIC granites

Fig. 9 Geological sketch map

showing the location of

geophysical profiles at the

Uhlırsky vrch. OIC ‘‘Older

Igneous Complex’’, YIC‘‘Younger Igneous Complex’’

554 Int J Earth Sci (Geol Rundsch) (2010) 99:545–565

123

Figure 11 highlights the variations of major oxides

(Table 4) in dioritic rocks and the granites (Fiala 1968) and

compares them with literature data on redwitzites in

Bavaria (Siebel 1993) and the Krusne hory/Erzgebirge

(Kovarıkova et al. 2007) indicated as contours of fields.

Dioritic rocks and granites show in the Harker diagrams

two different populations with a larger scatter of data

points for dioritic rocks. There is no distinct correlation

between major oxides and SiO2. The FeOtot, MgO and CaO

contents display generally negative trends whereas Na2O

contents versus SiO2 are positively correlated (Fig. 11).

Plots of quartz monzodiorite and granodiorite corre-

spond well with the fields of redwitzites from NE Bavaria

(Siebel 1993), while sample Lo4 better fits the Abertamy

gabbronorite (Kovarıkova et al. 2007). Large scatter of

major element oxide values shows the geochemical hete-

rogeneity of the individual rock types, which can be

attributed to various degree of mixing (see below), irreg-

ular presence of mafic cumulates in some mafic members

and uneven effects of deuteric alteration.

In the Harker diagrams, the quartz diorite/quartz mon-

zodiorite fields partly overlap with the field of granodiorite

for some oxides (Al2O3, FeOtot, K2O) but do not continue

coherently to the field of granites (Fig. 11). Thus, silica

rich granodiorites, compositionally close to the granites,

are missing as it is the case for majority of plutonic bodies

in the Krusne hory/Erzgebirge batholith.

Trace elements

Trace element composition of dioritic rocks is shown in

Table 4. Rb contents vary in a very narrow range (104 and

154 ppm) with a value of 119 ppm for the gabbronorite. Sr

concentrations change more broadly, the highest value

(891 ppm) is in quartz diorite, intermediate values

(393–605 ppm) are in quartz monzodiorite, and low values

(373–424 ppm) in granodiorite, the lowest Sr content

(202 ppm) was determined in gabbronorite.

Compatible trace element concentrations (Co, Cr, Ni)

are highly variable in all dioritic intrusions and correlate

positively with MgO. The gabbronorite (sample Lo4 in

Table 4) has very high Cr and Ni contents (1,138 and

201 ppm, respectively) and is geochemically exceptional

among the dioritic rocks of the Slavkovsky les.

All samples display a similar pattern in spider diagrams

(Fig. 12) normalized to primitive mantle. Figure 12a, b

compares the patterns of redwitzites from NE Bavaria

(Siebel 1993) and gabbronorite from Abertamy (Kovarıkova

0 100 200 300 400 500 600 700 800

x (m)

0

1

2∆ g

(m

Ga

l)

Gravity ∆g

Magnetics ∆TTopography H

-20

-10

0

10

20

30

40

50

∆T (

nT

)

700710720730740

H (

m)

a.s.

l.

0 100 200 300 400 500 600

x (m)

0

1

2

∆ g (

mG

al)

-20

-10

0

10

20

30

40

50

∆T (

nT

)

700710720730740

H (

m)

a.s.

l.

Profile 1 Profile 2

W E S N

Profile 1

)slaG

m(ytivar

G

0.2

0.4

0.6

0.8

1.0

1.2

Observed

Calculated

0 100 200 300 400 500 600

Distance (meters)V.E.=0.2

)srete

m(htpe

D.l.s.a

0

250

500

750

1000

D=2600D=2670

D=2760

700

Profile 2

)slaG

m(ytiv ar

G

0.2

0.4

0.6

0.8

1.0

1.2

0 100 200 300 400 500

Distance (meters)V.E.=0.2

)srete

m(htpe

D.

l.s.a0

250

500

750

1000

D=2760

0762=D0062=D

EW NS

Observed

Calculated

paragneiss granite

quartz monzodiorite quartz monzodiorite

granite paragneiss

Fig. 10 Results of gravity and magnetic measurements at the Uhlırsky vrch. Densities of geological blocks are given in kg/m3. V.E. vertical

exaggeration

Int J Earth Sci (Geol Rundsch) (2010) 99:545–565 555

123

Table 4 Major element oxides (in wt.%) and trace element composition (in ppm) of dioritic rocks from the Slavkovsky les

Sample Lo1 Lo2 Lo3 Lo4 Vı1 Hr1 Be1 Be2 Be3Type Qd Qmd Qmd gn Qmd grd grd grd grd

SiO2 51.00 52.92 56.76 52.48 55.93 60.34 60.98 60.18 59.34

TiO2 1.21 1.47 1.05 0.86 0.61 1.12 1.19 1.22 1.29

Al2O3 15.44 16.89 14.87 15.00 15.46 16.92 16.57 15.89 16.87

Fe2O3 2.03 1.71 1.36 1.63 1.74 1.49 1.08 2.21 1.76

FeO 6.14 6.19 5.16 6.26 4.91 4.04 4.22 4.15 4.35

MnO 0.15 0.14 0.11 0.16 0.11 0.08 0.09 0.09 0.09

MgO 7.10 5.40 7.51 9.00 8.16 3.71 3.78 3.99 3.95

CaO 7.52 7.11 5.17 8.12 4.43 4.74 4.32 4.20 4.41

Na2O 2.46 2.53 2.12 1.08 2.40 3.21 2.92 2.84 3.03

K2O 3.48 2.88 2.78 1.46 3.11 2.69 2.82 2.79 2.78

P2O5 0.64 0.44 0.40 0.18 0.34 0.34 0.32 0.38 0.34

H2O? 2.02 1.83 2.00 0.16 2.27 1.13 1.37 1.47 1.26

H2O- 0.16 0.08 0.14 0.10 0.10 0.06 0.06 0.10 0.14

CO2 0.12 0.01 0.05 2.64 0.05 0.08 0.02 0.12 0.06

F 0.11 0.18 0.12 0.10 0.10 0.13 0.10 0.10 0.10

-0 = 2F 0.05 0.07 0.05 0.04 0.04 0.05 0.04 0.04 0.04

Total 99.53 99.70 99.55 99.79 99.68 100.02 99.80 99.69 99.73

A/CNK 0.72 0.84 0.94 0.83 1.01 1.01 1.05 1.04 1.05

mg 60.88 55.16 67.72 67.47 69.44 54.85 56.10 53.53 54.06

Ba 2,643 1,922 1,438 480 1,133 1,002 1,065 992 1,268

Rb 118 113 129 119 154 115 104 122 113

Sr 891 605 463 202 393 424 391 373 421

Y 27.1 26.1 20.0 15.3 21.6 18.0 25.5 21.9 15.9

Zr 266 211 220 110 206 270 224 210 200

Nb 22.4 20.3 13.5 8.3 17.0 16.2 16.8 17.6 19.6

Th 15.6 11.3 17.3 6.1 20.8 12.0 6.8 15.2 6.2

Ni 35.0 18.1 44.6 200.8 132.2 18.6 29.1 44.7 24.6

V 215.6 205.2 161.5 217.0 119.8 99.7 117.4 121.1 128.7

Cr 178 116 390 1,138 400 86 128 128 123

Hf 7.5 6.2 6.7 3.3 6.2 7.3 6.1 5.9 5.6

Cs 8.3 6.7 11.2 33.5 8.6 83.2 5.7 10.0 9.4

Ta 1.7 1.4 1.1 0.7 1.2 0.9 0.9 1.0 1.1

Co 23.9 21.4 24.2 50.2 26.8 14.2 16.1 18.4 15.3

La 53.2 49.8 34.3 21.2 53.4 44.0 30.5 43.1 47.2

Ce 113.4 95.1 76.7 43.1 103.0 83.2 64.3 84.3 60.1

Pr 15.1 12.0 10.0 5.5 12.5 10.1 8.8 10.2 10.5

Nd 59.3 45.5 40.1 21.2 45.6 36.8 34.8 37.9 38.5

Sm 10.8 8.5 7.5 4.3 8.0 7.1 7.2 7.0 6.9

Eu 2.2 2.2 1.4 1.2 1.7 1.8 1.9 2.0 1.9

Gd 6.0 5.0 4.0 2.5 4.6 4.2 4.3 4.3 4.0

Tb 1.08 0.96 0.75 0.54 0.85 0.76 0.90 0.79 0.77

Dy 5.4 5.1 3.9 3.0 4.4 3.9 4.9 4.3 3.9

Ho 1.05 0.98 0.71 0.61 0.84 0.73 0.98 0.83 0.70

Er 3.0 2.8 2.1 1.7 2.4 1.9 2.8 2.3 1.7

Tm 0.41 0.38 0.29 0.23 0.32 0.24 0.37 0.32 0.21

Yb 2.6 2.6 2.5 1.9 2.1 1.5 2.3 2.0 1.4

Lu 0.39 0.39 0.36 0.28 0.30 0.21 0.33 0.29 0.21

(La/Yb)N 13.8 12.9 9.2 7.5 17.1 19.8 8.9 14.5 22.7

Eu/Eu* 0.76 0.95 0.71 1.03 0.79 0.93 0.97 1.04 1.02

A/CNK = Al2O3/(CaO ? Na2O ? K2O), mg = 100 Mg/(Mg ? Fetotal), Eu/Eu* = EuN/{(SmN ? GdN)/2}

Explanation of samples: Qd quartz diorite from Uhlırsky vrch and from quarry Vıtkov, Qmd quartz monzodiorite from the Lobzy brook valley,gn gabbronorite from the Lobzy brook valley, grd granodiorite from Hruskova (N of Becov) and from Becov

556 Int J Earth Sci (Geol Rundsch) (2010) 99:545–565

123

et al. 2007) with those for dioritic intrusionions in the

Slavkovsky les. The diagrams show a trend of enrichment in

incompatible elements (Cs, Ba and Th), slight depletion of

Rb and strong depletion of Nb. Variously displayed are

minor troughs for Sr and Ti. The gabbronorite (sample Lo4)

significantly differs in the amounts of trace elements. It has

lower contents of lithophile elements (Rb, Ba, Th, Sr) and

REE, but higher transitional elements (Cr, Ni) and shows a

very pronounced Nb through.

Figure 13a, b highlights the REE patterns of dioritic

rocks of the Slavkovsky les in comparison with the

redwitzite from NE Bavaria (Siebel 1993) and gabbro-

norite from Abertamy (Kovarıkova et al. 2007). All

dioritic rocks examined have a similar REE distribution

with the predominance of LREE over HREE. The HREE

show a characteristic flat slope. The (La/Yb)N ratio

varies from 1.7 to 5.2 and no obvious Eu anomaly is

apparent. Dioritic intrusions from the Slavkovsky les

show higherP

REE concentrations compared to gabbro-

norites from Abertamy (Kovarıkova et al. 2007) and fit

well with the field of redwitzites (Siebel 1993). The

sample of gabbronorite (Lo4) has noticeably lower REE

contents and it is well comparable with the gabbronorite

from Abertamy.

Geothermometry and geobarometry

Zirconium concentration in the studied dioritic intrusions

ranges between 200 and 270 ppm (Table 4) and it is

0.0

0.5

1.0

1.5

2.0

2.5

TiO

2

1014

1822

Al 2O

3

24

68

10

Fe

Oto

t

05

1015

Mg

O (

wt.

%)

24

68

CaO

(w

t. %

)

12

34

Na

2O (

wt.

%)

45 50 55 60 65 70 75

12

34

56

K2O

(w

t. %

)

SiO2

45 50 55 60 65 70 75

0.2

0.4

0.6

0.8

1.0

P2O

5

granodiorite

quartz diorite

quartz monzodiorite

45 50 55 60 65 70 75

0.0

0.2

0.4

0.6

0.8

F (

wt.

%)

(wt. %) SiO2 (wt. %) SiO2 (wt. %)

(wt.

%)

(wt.

%)

(wt.

%)

(wt.

%)

quartz monzodiorites andquartz diorites

granodiorites

granites OIC + YIC

This study

Fiala (1968)

granodiorite

diorite

gabbrodiorite

granite

redwitzites NE Bavaria

gabbronorite, gabbrodioriteAbertamy

gabbronoriteFig. 11 Harker variation

diagrams for dioritic intrusions

and associated granites from the

Slavkovsky les; data from this

study and Fiala (1968)

Cs Rb Ba Th Nb K La Ce Pr Sr P Nd Zr Sm Eu Ti Dy Y Yb Lu V Cr Ni

0.00

10.

010.

11

1010

010

0010

000

Sam

ple/

prim

itive

man

tle

Cs Rb Ba Th Nb K La Ce Pr Sr P Nd Zr Sm Eu Ti Dy Y Yb Lu V Cr Ni

0.00

10.

010.

110

100

1000

1000

0

Sam

ple/

prim

itive

man

tle

quartz diorite

quartz monzodiorite

redwitzite NE Bavaria

gabbronorite Abertamy

granodiorite

redwitzite NE Bavaria

gabbronorite Abertamy

gabbronorite

a b1

Fig. 12 Spider diagrams for dioritic intrusions in the Slavkovsky

les compared with the redwitzites from NE Bavaria (Siebel 1993)

and gabbronorites from Abertamy (Kovarıkova et al. 2007);

a gabbronorite, quartz diorite and quartz monzodiorites from the

Slavkovsky les; b granodiorites from the Slavkovsky les. Normalized

to primitive mantle values (Taylor and McLennan 1986)

Int J Earth Sci (Geol Rundsch) (2010) 99:545–565 557

123

considerably lower in the gabbronorite (110 ppm). These

values correspond to zircon crystallization temperatures

between 730 and 770�C according to the zircon saturation

model by Watson and Harrison (1983). The temperature

range is lower than that reported for gabbrodiorite and

gabbronorite from Abertamy (Kovarıkova et al. 2007)

(800–860�C) and the redwitzites from NE Bavaria

(\860�C; Siebel et al. 2003). The granodiorite yields a

higher zirconium saturation temperature of about 800�C.

Low zircon saturation temperatures may suggest that the

parental melt was probably not Zr-saturated or was

Zr-saturated only for a limited period untill the source was

exhausted (Watson and Harrison 1984).

Apatite saturation temperatures calculated using the

model of Harrison and Watson (1984) provide the tem-

peratures ranges of about 750�C for gabbronorite, 895�C

for quartz diorite, 870–910�C for quartz monzodiorite and

740–810�C for granodiorite. They are about 50–100�C

higher than the temperatures calculated from the zircon

thermometry.

The equilibration temperatures determined from the

amphibole-plagioclase pairs according to Holland and

Blundy (1994) are, on average, 845�C for quartz monzo-

diorite, 835�C for quartz diorite and 785�C for granodiorite.

All these temperatures are similar to the temperatures cal-

culated from the apatite saturation model.

To determine the pressure during the crystallization, we

used the Al-in-hornblende geobarometer based on a linear

variation of Al contents in hornblende with the pressure of

crystallization (Hammarstrom and Zen 1986; Hollister

et al. 1987; Johnson and Rutherford 1989; Schmidt 1992).

The average values obtained using these models are 2.2

kbar for quartz monzodiorite, 1.6 kbar for quartz diorite

and 1.4 kbar for granodiorite.

Geochronology

Zircons separated from the Uhlırsky vrch quartz monzo-

diorite and the Becov granodiorite were analysed by

the single-zircon Pb-evaporation technique. Five zircon

grains from the quartz monzodiorite gave an age of

323.4 ± 4.4 Ma (Table 5; Fig. 14). The granodiorite from

Becov gave zircon Pb-evaporation ages of 327.7 ± 3.7 Ma

(weighted mean of five grains) and 326.1 ± 5.1 Ma

(weighted mean of three out of five grains—two grains

excluded from mean age calculation due to their higher

common Pb content—see Table 5). These ages are com-

parable with those of dioritic intrusions from Abertamy

(Kovarıkova et al. 2007) as well as with the redwitzites

associated with the Leuchtenberg granite and from the

type-locality Marktredwitz (Siebel et al. 2003) and similar

to the OIC granites from Abertamy (322.8 ± 3.5 Ma;

Kovarıkova et al. 2007). However, the age data do not

allow defining an intrusion sequence since the quartz

monzodiorite and the granodiorite are not in geological

contact and the age data overlap within the uncertainties of

measurements.

Zircon dating of the YIC granite near the contact with

the quartz monzodiorite from the Uhlırsky vrch did not

yield well-constrained results because of the high common

Pb component hosted in zircons from this sample. Three

grains with the highest measured 206Pb/204Pb ratios

(*400–1,600) yielded a 207Pb/206Pb-evaporation date of

321 ± 6 Ma. This age is similar to the age of the YIC

granites measured in the Nejdek-Eibenstock pluton

(320 ± 8 Ma, Kempe et al. 2004) and also accords with a

U–Pb monazite age of 321 ± 3 Ma reported by Forster

et al. (1999) for two samples of the megacrystic Eibenstock

granite.

La C e Pr Nd Pm S m E u Gd Tb Dy Ho E r Tm Yb Lu

110

100

1000

Sam

ple/

chon

drite

110

100

1000

Sam

ple/

chon

drite

La C e Pr Nd Pm S m E u Gd Tb Dy Ho E r Tm Yb Lu

quartz diorite

quartz monzodiorite

granodiorite

redwitzite NE Bavaria

gabbronorite Abertamy

redwitzite NE Bavaria

gabbronorite Abertamy

gabbronoritea b

Fig. 13 Chondrite normalized (Boynton 1984) REE diagram for

dioritic rocks from the Slavkovsky les compared to the redwitzites

from NE Bavaria (Siebel 1993) and gabbronorites from Abertamy

(Kovarıkova et al. 2007); a quartz diorite and quartz monzodiorite

from the Slavkovsky les; b granodiorite from the Slavkovsky les

558 Int J Earth Sci (Geol Rundsch) (2010) 99:545–565

123

Discussion

Mafic and intermediate intrusions revisited in the Slav-

kovsky les show a close compositional identity with the

redwitzites in the Northern Obepfalz as indicated by min-

eral composition, textures, major and trace element

geochemistry and age of emplacement. We use the term

‘‘dioritic intrusions’’ to denote their overwhelming

petrographical nature of them except for a single occur-

rence of a gabbroic rock classified as gabbronorite.

Dioritic intrusions are spatially associated with late

Variscan granites of the Western Krusne hory/Erzgebirge

granite pluton. They occur as sills, minor tabular bodies

and dykes in sizes of several dm up to tens of meters,

exceptionally to hundreds of meters, in metasediments of

the Slavkovsky les Crystalline Unit near the contacts of

Fig. 14 Histograms showing

the distribution of radiogenic207Pb/206Pb ratios from zircon

grains of samples Lo-2 (quartz

monzodiorite, Uhlırsky vrch)

and Be-3 (granodiorite, Becov)

Table 5 Results of single

zircon 207Pb/206Pb* evaporation

analyses (for geochemical

composition of samples see

Table 4)

207 Pb/206Pb* corrected for

common Pb

No. of 207Pb/206Pb*

ratios

204Pb/206Pb 206Pb/208Pb U/Th 207Pb/206Pb* Age (Ma)

Q monzodiorite

Lo2/grain2 201 0.000109 3.2 1.0 0.052997 328.7 ± 3.4

Lo2/grain3 347 0.000071 5.4 1.7 0.052786 319.7 ± 2.8

Lo2/grain4 127 0.000060 3.3 1.0 0.052894 324.3 ± 3.1

Lo2/grain5 240 0.000164 3.6 1.1 0.052925 325.6 ± 3.5

Lo2/grain6 318 0.000057 5.0 1.6 0.052823 321.2 ± 3.0

W. avg. 323.4 ± 4.4

Granodiorite

Be3/grain1 131 0.000049 7.9 2.5 0.052918 325.3 ± 4.1

Be3/grain4 136 0.000094 5.4 1.7 0.052993 328.5 ± 3.6

Be3/grain5 239 0.000091 5.1 1.6 0.052895 324.3 ± 3.5

W. avg. (3 grains) 326.1 ± 5.6

Be3/grain6 155 0.000481 5.5 1.6 0.053057 331.3 ± 4.0

Be3/grain7 201 0.000242 5.8 1.8 0.053027 330.0 ± 4.2

W. avg. (5 grains) 327.7 ± 3.7

Int J Earth Sci (Geol Rundsch) (2010) 99:545–565 559

123

younger suite granites. Granodiorites are restricted to the

older granite suite and they outcrop remote from the

present granite contact. Dioritic intrusions are usually

compositionally different in various spatially distant

localities and variable in some single minor bodies or sills.

Largest exposures of quartz diorites and monzodiorites are

spatially associated with the NW contact of the Krudum

massif where a gabbroic rock showing a textural and

compositional resemblance with the gabbronorites from

Abertamy (Kovarıkova et al. 2007) was found.

As dioritic intrusions have mostly sharp intrusive con-

tacts with the host metasedimentary rocks, we interpret

their position as posttectonic, postdating the tectonic

stacking of the major rock units on the Saxothuringian—

Tepla-Barrandian boundary. Their position at the contact

zone of the granites and their crystallization history indi-

cate that they were solidified in shallow levels and

crystallized at pressures \2 kb. However, the geological

evidence in the study area does not allow (due to poor

outcrops) distinguishing whether the intrusion of mafic

rocks and granites proceeded in succession or that they

were emplaced contemporaneously. Their crystallization

interval of temperatures from 770 to 900�C is higher than

that of granites and overlaps that determined for the

Bavarian redwitzites.

Present geochronological data (323 Ma for quartz

monzodiorite and 326 Ma for granodiorite) unequivocally

place the origin of dioritic intrusions into the late Variscan

time and proves their contemporaneity with the 325 Ma old

granites of the Western Krusne hory/Erzgebirge pluton

(Kempe et al. 2004; Romer et al. 2007) or redwitzites in the

Northern Oberpfalz (Siebel et al. 2003).

Fiala (1968) proposed for the Slavkovsky les dioritic

rocks that assimilation of earlier emplaced solid mafic

rocks by younger granitic magmas could produce some

dioritic compositions. This observation appears to be sup-

ported by the occurrences of dioritic sills spatially

associated with granite or pegmatite dykes and commonly

interlayered with these rocks. However, in accordance with

our new geological and geochemical data we explain dio-

ritic and granitic compositions as formed by separate

magmatic pulses without any interaction between the solid

diorite and granite magma at the site of emplacement.

We suggest that mafic magmas participated at the origin

of granitoids in the Western Krusne hory/Erzgebirge

granite pluton not only by the heat of their intrusions but

also by the addition of the mantle component to the crustal

melts in initial stages of granitic magmatism. Dioritic

intrusions are typical K-rich rocks and their strong

enrichment in LILE and REE indicates an affinity to K-rich

calc-alkaline magmas (Gerdes et al. 2000; Janousek et al.

2000; Guo et al. 2004) commonly generated by melting of

a metasomatically enriched mantle source (Fraser et al.

1985; Nelson 1992). Various enriched mantle-derived

mafic igneous rocks with a crustal-like isotope composition

are a characteristic feature of Variscan magmatism (Holub

1997; Mendes and Dias 2004; Solgadi et al. 2007) in the

Central European Variscides. Redwitzites from NE Bavaria

show typically crustal-like isotope composition (Taubald

2000; Gerdes et al. 2000; Siebel et al. 2003) that together

with a strong enrichment of large ion lithophile elements

and LREE and with flatter HREE pattern indicates a geo-

chemical affinity to K-rich calc-alkaline magmatism.

The sample of gabbronorite (Lo4) whose mafic com-

position appears to be the closest to a possible primary

mafic magma is not suitable as a mafic parental magma as

Table 6 Chemical composition of mafic magmas and granite OIC

used as end members for models of mixing and FC

OIB SAB CAL GR

SiO2 47.63 46.44 49.25 72.42

TiO2 2.45 2.63 1.80 0.27

Al2O3 12.63 15.06 13.95 13.98

FeOt 11.57 11.63 9.25 1.42

MnO 0.18 0.18 0.10 0.03

MgO 11.20 7.83 7.10 0.89

CaO 9.82 9.96 6.95 1.15

Na2O 2.39 3.72 3.20 3.52

K2O 0.65 1.56 2.80 4.71

P2O5 0.31 0.74 0.65 0.12

Rb 13.38 41.61 98.50 217.00

Ba 186.00 625.00 942.00 550.00

Th 1.41 8.68 12.70 27.10

Nb 19.80 65.10 18.00 14.40

La 17.32 47.50 35.59 46.63

Ce 41.21 96.50 83.15 90.63

Pr – 6.96 9.88 10.75

Sr 411.20 934.57 1,118.00 150.50

Nd – 43.41 43.02 37.60

Zr 176.80 231.71 282.50 139.50

Sm 6.10 8.23 8.57 7.11

Eu 1.97 2.63 1.80 0.85

Dy – 5.35 3.74 5.27

Y 23.70 30.92 30.00 29.48

Yb 1.99 2.16 1.43 3.26

Lu 0.29 0.32 0.18 0.46

V – 208.60 – 18.00

Cr 673.60 228.86 334.5 25.50

Ni – 135.00 172.5 26.50

Main oxides are in wt.%, trace elements in ppm

OIB ocean island basalt, selected samples under 50% SiO2 (BVSP

1981). SAB continental sodic-alcali basalt (Kelemen et al. 2004).

CAL calc-alkline lamprophyre, selected samples under 50% SiO2

(Jargalan et al. 2007). GR granite OIC (Kovarıkova et al. 2007)

560 Int J Earth Sci (Geol Rundsch) (2010) 99:545–565

123

it has a cumulate character. This sample has high amounts

of Cr, Ni, Co and low contents of incompatible elements,

especially Ba and Sr. Higher content of Rb and Cs in this

sample is probably caused by secondary enrichment.

We used three different enriched mantle-derived mag-

mas reported in the literature as mafic end members to

document the differences between various sources and to

select the most suitable one: (a) calc-alkaline lamprophyre

from Mongolia (CAL; Jargalan et al. 2007); (b) continental

sodic-alkali basalt from Turkey (SAB; Kelemen et al.

2004); (c) Hawaian ocean island basalts [OIB; Basaltic

Volcanism Study Project (BVSP) 1981]. For the calcula-

tion, we used average values of basalts and lamprophyres

with an SiO2 content that is lower than in dioritic intrusions

(Table 6).

We calculated the amounts of felsic component parti-

cipating in mixing process using major element oxides. As

felsic parental magmas we used an average OIC granite

(Kovarıkova et al. 2007), representing the least differenti-

ated silicic magma in the study area (Table 6). The

percentage contributions of granitic melt derived from the

mixing calculation are 21–25% for quartz diorite, 30–35%

for quartz monzodiorite and 49–53% for granodiorite.

Figure 15 shows the plots of mixing relationship to each

rock type and the relevant portion of granitic magma

involved. The diagrams are pictured independently for each

type of mafic end member (CAL, SAB and OIB). Values

for granodiorite plot fairly well on the mixing line for all

mafic end members. Plots of the other samples (quartz

diorite and quartz monzodiorite) show large scatter sug-

gesting an involvement of other petrogenetic processes.

The results of magma mixing and fractional crystalli-

zation modelling are shown in Fig. 16a–c. Changes in trace

element compositions are plotted in spider diagrams. Fields

in different shades of grey represent individual dioritic

intrusions. The black lines show calculated trace element

a)

b)

c)

Fig. 15 Ch-Cb versus Ca-Cb diagrams (according to Fourcade and

Allegre 1981) for dioritic intrusions from the Slavkovsky les. The

diagrams are separate for each type of intrusion in the Slavkovsky les

and each mafic end member a calc-alkaline lamprophyre (CAL;

Jargalan et al. 2007); b continental sodic-alkali basalt (SAB; Kelemen

et al. 2004); c ocean island basalts (OIB; BVSP 1981). Ca concen-

tration of an element in the acid parental magma, Cb concentration in

the mafic parental magma, Ch concentration in the calculated hybrid

Int J Earth Sci (Geol Rundsch) (2010) 99:545–565 561

123

composition of hybrid rock that originated by mixing of

mafic and felsic magma (shown are the lines for 20 and

53% of felsic component participating in the mixing). The

black/white line shows the composition after 30% frac-

tional crystallization (FC) of 80% of clinopyroxene and

20% of plagioclase. The black/grey line documents the

composition after 30% FC that followed after mixing

(shows the line for 35% of felsic component participating

in the mixing).

OIB (BVSP 1981) as a mafic end member gives insuf-

ficient amounts of trace elements (Rb, Ba, Sr, Zr) needed to

form hybrid rocks corresponding to dioritic intrusions of

the Slavkovsky les. The calculated lines for SAB (Kelemen

et al. 2004) as mafic end member yield a better overlap

with the dioritic intrusions. However, the Nb anomaly for

SAB is slightly positive or weakly negative. This anomaly

is strongly negative in the dioritic intrusions. CAL

(Jargalan et al. 2007) as a mafic end member shows the

best overlap with the dioritic intrusions except of some

REE (Eu, Yb). Thus, a mafic magma of calc-alkaline

lamprophyre composition seems to be the most likely

parental magma for the dioritic intrusions in the Slav-

kovsky les. This concept revives the original idea by

Willmann (1920) pointing to a resemblance of redwitzites

with lamprophyres. However, dioritic intrusions do not

form simple and continuous lines on binary compositional

diagrams and their composition cannot be derived only

from mixing or fractional crystallization. It is probable that

the mafic parental magma was heterogeneous and different

portions of mafic magma underwent diverse stages of

fractional crystallization. Then these portions of fraction-

ated magma interacted with co-existing granitic magmas.

The new data on dioritic rocks from the Slavkovsky les

give some additional arguments for a more significant role

of mafic magmas as the heat sources and components in the

genesis of Late Variscan granites during the Variscan

orogeny. The position of the dioritic intrusions in the

broader contact zones of granitic bodies strongly favours

their role as forerunners of a more massive granitic mag-

matism. Dioritic intrusions used the initial pathways that

Rb Ba Th Nb La Ce Sr Zr Sm Eu Y Yb Lu

Sam

ple/

chon

drite

Rb Ba Th Nb La Ce Sr Zr Sm Eu Y Yb Lu

Rb Ba Th Nb La Ce Sr Zr Sm Eu Y Yb Lu

gabbronorite

granodiorite

quartz diorite

quartz

monzodiorite

a OIB b SAB

c CAL

mixing lines (16% and 53% of acid component)

30% FC

30% FC after mixing (35% of acid component

participated in mixing)

110

100

1000

Sam

ple/

chon

drite

110

100

1000

Sam

ple/

chon

drite

110

100

1000

Fig. 16 Chondrite-normalized (normalizing values according to

Boynton 1984) trace element patterns illustrating the modelling of

mixing (black lines), fractional crystallization of clinopyroxene

(80%) ? plagioclase (20%) (black/white lines) and fractional crys-

tallization after mixing (black/grey lines). The models are calculated

for three different mafic end members a calc-alkaline lamprophyre

(Jargalan et al. 2007); b sodic-alkali basalt (Kelemen et al. 2004);

c ocean island basalt (BVSP 1981). Average OIC granite was used as

felsic end member in all cases

562 Int J Earth Sci (Geol Rundsch) (2010) 99:545–565

123

were subsequently used by voluminous granitic magmas

during the repeated late Variscan magmatic activity. The

magmas apparently mixed in the deeper-seated chambers

in the lower crust, but fractional crystallization of intruded

melts was effective in the upper crust near or at the sites of

their emplacement and contributed to the compositional

variability of dioritic rocks.

Conclusions

Dioritic intrusions of the Slavkovsky les are equivalents of

redwitzites from NE Bavaria. Zircon geochronology shows

that they were emplaced at c. 325 Ma and are broadly

contemporaneously with the intrusion of late Variscan

granites of the Krusne hory/Erzgebirge batholith. Our

geochemical data support the concept that they are prod-

ucts of interaction between mafic and felsic melts

accompanied or preceded by fractional crystallization of

mafic or mixed melts. The lamprophyric or alkali basalt

melts derived from a metasomatically altered upper mantle

are considered as suitable mafic end members capable to

explain most of the compositional variations. Thus, mafic

magmatism probably affected the sources of Late Variscan

granites of the Krusne hory/Erzgebirge batholith also in the

area of the Western Krusne hory/Erzgebirge pluton in the

NW part of the Bohemian Massif.

Acknowledgments The work was done under the financial support

of the projects 205/02/0458, 205/05/0156 of the Grant Agency of the

Czech Republic and Scientific Project of Ministry of Education,

Youth and Sports CR No. 0021620855. David Dolejs is gratefully

thanked for helpful discussion. We appreciate the comments of three

anonymous reviewers who significantly improved the original version

of the manuscript.

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