Geochemistry of Granitic Rocks of the Moldanubian Batholith (Central European Variscides)

*Miloš René*

#### **Abstract**

Granitic rocks of the Moldanubian batholith are represented by four magmatic suites: I- to S-type Weinsberg biotite granites-granodiorites, S-type Eisgarn two-mica granites, S-type Melechov/Zvůle two mica, highly fractionated granites and I/S-type Freistadt biotite granites-granodiorites. The biotite granites of the Weinsberg suite are subaluminous to weakly peraluminous granites, enriched in Ba, Sr, and Zr. The two-mica granites of the Eisgarn suite are represented by a peraluminous, the low-Th Deštná granites, intermediate-Th Mrákotín, Číměř/ Aalfang granites, and the high-Th Lipnice/Steinberg granites. The alkali feldspar and two-mica granites of the Melechov/Zvůle suite are highly fractionated, peraluminous granitic rocks, depleted especially in Ba, Zr, and Th. The granites to granodiorites of the Freistadt suite are subaluminous on Ba- and Sr-enriched granitic rocks.

**Keywords:** granitic rocks, petrology, geochemistry, Moldanubian zone, Bohemian Massif

#### **1. Introduction**

Generation of granitic rocks batholiths and plutons is a characteristic late-stage feature in the evolution of collisional orogens [1–4]. One of the classic examples is the European Variscan Belt, produced as a result of the late Palaeozoic convergence of Gondwana and Laurussia. The Moldanubian batholith that forms one of the largest plutonic complexes within the European Variscan Belt, covering 10,000 km<sup>2</sup> in the central part of the Moldanubian Zone of the Bohemian Massif, provides an excellent insight into origin and evolution of such crustally derived magmas [5–10]. The most significant previous geochemistry studies of the Moldanubian batholith are concentrated in papers Liew et al., Vellmer and Wedepohl, and Breiter [5, 6, 9]. However, these papers are concentrated only on selected parts (the Austrian and South Bohemian) of this batholith.

The aim of the presented paper is detailed classification of individual magmatic suites of the whole Moldanubian batholith and description of petrology, geochemistry, and origin of its magmatic suites.

#### **2. Geological setting**

In map view, the Moldanubian batholith resembles a "V" shape having two nearly perpendicular segments oriented ~NNE-SSW and ~NW-SE (**Figure 1**). The ~NNE-SSW trending segment as the eastern part of the batholith is formed by large continuous exposures of granitic rock pluton, whereas the ~NW-SE as the western part of the batholith is formed by a number of isolated smaller plutons and bodies, some of which seem to be roughly parallel to the ~NW-SE trending regional shear zones (the Pfahl and Danube shear zones [13–15]). Both batholith branches are closely associated with the host migmatites [10, 16, 17]. Estimates of the pluton emplacement depths range from a number of separate smaller plutons, some of which seem to be from 18 to 20 km in the NW-SE segment and/or 7 to 9 km in the NNE-SSW segment of the Moldanubian batholith [10, 12].

The most significant S-type granites of the Eisgarn suite occurred in the NNE-SSW branch of the Moldanubian batholith are hosted in a complex of cordieritebearing migmatites and migmatitized paragneisses of the Pelhřimov complex [16].

The batholith consists of multiple intrusive units (plutons and stocks), predominantly composed of felsic to intermediate, granitic to granodioritic rocks with either S- or transitional I/S-type character [5, 6, 8, 9, 18]. All these granitoids can be classified into four main suites [6, 8, 9]:


Klötzli et al. [23] proposed that the origin of the Moldanubian batholith begun with the partial melting of mid—to lower crustal pre-Variscan rocks, polyphase

**5**

**Figure 1.**

*Geochemistry of Granitic Rocks of the Moldanubian Batholith (Central European Variscides)*

exhumation, anatexis, and deformation, closely followed by emplacement of large volumes S/I-type and S-type granodiorites and granites between 331 and 326 Ma. According to the high-precision ID-TIMS U-Pb zircon and monazite dating the oldest Weinsberg granite (330.7 ± 0.4 Ma) intruded in southern part of the ~NNE-SSW segment of the Moldanubian batholith. Neighbouring two-mica granites of the Eisgarn suite were dated at 327.0 ± 0.3 Ma (Mrákotín variety), 327.14 ± 0.21 Ma (Deštná variety), and 328.5 ± 2.1 Ma (Číměř/Aalfang variety). However, the Weinsberg granite in the ~NW-SE segment of the Moldanubian batholith is comparably younger (327.7 ± 0.4 to 325.75 ± 0.39 Ma). The two-mica granite of the Eisgarn suite from this magmatic segment in the Lipno/Sternstein pluton was dated at 326.4 ± 0.6 Ma. Thus, the NW-SE segment of the Moldanubian batholith was formed ~3 Ma later than the NNE-SSW segment. However, the Weisberg granite from southern part of NW-SE segment, south of the Pfahl fault, was dated at 322.7 ± 0.7 Ma, implying that the processes of crustal melting migrated in the area of the Moldanubian batholith further toward south with time [24]. These U-Pb ages of granitoid rocks occurred in the NW-SE segment of the Moldanubian batholith and their structural relations with the Pfahl shear zone indicate the initial stages of dextral shearing at c. 342–327 Ma and mylonitic deformation coeval with granite emplacement during c. 326–327 Ma [10, 24]. The I/S-type granodiorites of the Freistadt/Mauthausen suite are distinctly younger. Age of monazite from the Freistadt granodiorite is 302 ± 2 Ma [25], and the age of monazite from the fine-

*Geological map of the Moldanubian batholith (after [11, 12], modified by author).*

grained, I-type Mauthausen granite is 316 ± 1 Ma [26].

*DOI: http://dx.doi.org/10.5772/intechopen.93189*

*Geochemistry of Granitic Rocks of the Moldanubian Batholith (Central European Variscides) DOI: http://dx.doi.org/10.5772/intechopen.93189*

#### **Figure 1.**

*Geochemistry*

**2. Geological setting**

In map view, the Moldanubian batholith resembles a "V" shape having two nearly perpendicular segments oriented ~NNE-SSW and ~NW-SE (**Figure 1**). The ~NNE-SSW trending segment as the eastern part of the batholith is formed by large continuous exposures of granitic rock pluton, whereas the ~NW-SE as the western part of the batholith is formed by a number of isolated smaller plutons and bodies, some of which seem to be roughly parallel to the ~NW-SE trending regional shear zones (the Pfahl and Danube shear zones [13–15]). Both batholith branches are closely associated with the host migmatites [10, 16, 17]. Estimates of the pluton emplacement depths range from a number of separate smaller plutons, some of which seem to be from 18 to 20 km in the NW-SE segment and/or 7 to 9 km in the

The most significant S-type granites of the Eisgarn suite occurred in the NNE-SSW branch of the Moldanubian batholith are hosted in a complex of cordieritebearing migmatites and migmatitized paragneisses of the Pelhřimov complex [16]. The batholith consists of multiple intrusive units (plutons and stocks), predominantly composed of felsic to intermediate, granitic to granodioritic rocks with either S- or transitional I/S-type character [5, 6, 8, 9, 18]. All these granitoids can be

a.Coarse-grained, mainly porphyritic I- to I/S-type biotite granites to granodiorites of the Weinsberg suite including four subtypes (coarse-grained, porphyritic Weinsberg I, very coarse-grained porphyritic biotite to muscovitebiotite Weinsberg II, coarse-grained biotite-amphibole granite to granodiorite

b.S-type two-mica granites of the Eisgarn suite including the equigranular Mrákotín variety, porphyritic Číměř/Aalfang variety, highly porphyritic Lipnice/Steinberg variety and equigranular Deštná variety, occurred only in

d.Fine- to coarse-grained I/S-type-biotite granites and granodiorites of the Freistadt/Mauthausen suite including the coarse-grained "marginal variety," medium-grained "central variety" of the Freistadt pluton, and the muscovite bearing biotite granite of the Graben granite variety occurred only on the

Klötzli et al. [23] proposed that the origin of the Moldanubian batholith begun with the partial melting of mid—to lower crustal pre-Variscan rocks, polyphase

c.Younger group of highly fractionated, coarse-grained S-type two-mica granites of the Melechov/Zvůle suite formed ring-shaped bodies or stocks, often with zoned internal structure. From the NE to the SW, there are following bodies in the ~NNE-SSW segment of the Moldanubian batholith (the Melechov, Čeřínek, and Zvůle bodies). According to its geologic position, mineralogical and geochemical composition could be to these bodies attached also the coarsegrained, weakly porphyritic biotite-muscovite Plechý granite in central part of the Plechý pluton (Verner et al. [12]) and the fine-grained two-mica Sulzberg granite in the Bärenstein pluton of the ~NW-SE segment of the Moldanubian

"Schlieren granite" and slightly porphyritic Srní granite)

NNE-SSW segment of the Moldanubian batholith [10, 12].

classified into four main suites [6, 8, 9]:

the Klenov pluton

batholith [19] (**Figure 2**).

eastern margin of the Freistadt town [21, 22].

**4**

*Geological map of the Moldanubian batholith (after [11, 12], modified by author).*

exhumation, anatexis, and deformation, closely followed by emplacement of large volumes S/I-type and S-type granodiorites and granites between 331 and 326 Ma.

According to the high-precision ID-TIMS U-Pb zircon and monazite dating the oldest Weinsberg granite (330.7 ± 0.4 Ma) intruded in southern part of the ~NNE-SSW segment of the Moldanubian batholith. Neighbouring two-mica granites of the Eisgarn suite were dated at 327.0 ± 0.3 Ma (Mrákotín variety), 327.14 ± 0.21 Ma (Deštná variety), and 328.5 ± 2.1 Ma (Číměř/Aalfang variety). However, the Weinsberg granite in the ~NW-SE segment of the Moldanubian batholith is comparably younger (327.7 ± 0.4 to 325.75 ± 0.39 Ma). The two-mica granite of the Eisgarn suite from this magmatic segment in the Lipno/Sternstein pluton was dated at 326.4 ± 0.6 Ma. Thus, the NW-SE segment of the Moldanubian batholith was formed ~3 Ma later than the NNE-SSW segment. However, the Weisberg granite from southern part of NW-SE segment, south of the Pfahl fault, was dated at 322.7 ± 0.7 Ma, implying that the processes of crustal melting migrated in the area of the Moldanubian batholith further toward south with time [24]. These U-Pb ages of granitoid rocks occurred in the NW-SE segment of the Moldanubian batholith and their structural relations with the Pfahl shear zone indicate the initial stages of dextral shearing at c. 342–327 Ma and mylonitic deformation coeval with granite emplacement during c. 326–327 Ma [10, 24]. The I/S-type granodiorites of the Freistadt/Mauthausen suite are distinctly younger. Age of monazite from the Freistadt granodiorite is 302 ± 2 Ma [25], and the age of monazite from the finegrained, I-type Mauthausen granite is 316 ± 1 Ma [26].

#### **Figure 2.**

*Schematic geological map of the NW-SE segment of the Moldanubian batholith (after [20] modified by author).*

#### **3. Analytical methods**

Rock samples of 2–5 kg in weight were crushed in a jaw crusher and a representative split of these materials was ground in an agate ball mill. For geochemical study of analysed granitoids were used 75 representative rock samples (**Table 1**, **Figures 3**–**7**). Major elements and some trace elements (Ba, Rb, Sr, Zr, Nb, Y, U, and Th) were determined using a Bruker AXS S4 Pioneer X-ray fluorescence spectrometer at the University of Salzburg, Austria, on fused glass discs and pressed rock powder pellets, respectively. The FeO was determined by titration, H2O+ and H2O<sup>−</sup> were analyzed gravimetrically in the chemical laboratory of the Institute of Rock Structure and Mechanics, Academy of Sciences of the Czech Republic, Prague. Rare earth elements were quantified by inductive coupled plasma mass spectrometry (ICP-MS) techniques at Activation Laboratories Ltd., Ancaster, Canada, using a Perkin Elmer Sciex ELAN 6100 ICP mass spectrometer, following standard lithium metaborate/tetraborate fusion and acid decomposition sample preparative procedures.

Microprobe analyses of selected minerals (feldspars and biotite) were performed in polished thin sections using a CAMECA SX-100 microprobe operated in wavelengthdispersive mode at the Institute of Geology, Academy of Sciences of the Czech Republic. The raw analytical data were corrected using the PAP procedure [28]. Operation conditions were accelerating potential of 15–20 kV, beam current of 10–70 nA (measured on

**7**

**Figure 3.**

*Geochemistry of Granitic Rocks of the Moldanubian Batholith (Central European Variscides)*

**Zr ppm Th** 

Weinsberg Weinsberg I 1.5–3.0 214–441 19–45 269–443 10.0–30.5 0.30–0.60

Eisgarn Deštná 0.4–1.1 39–81 2–7 33–69 3.2–19.0 0.35–1.18

Freistadt Central 1.9–3.4 102–188 4–19 141–180 12.2–20.9 0.68–0.81

**ppm**

Weinsberg II 1.1–2.6 58–491 4–31 58–491 4.9–30.3 0.18–0.53 Schlierengranite 1.9–4.6 133–652 5–42 n.a. n.a. n.a.

Srní 1.5–4.3 190–331 25–31 266–430 12.6–33.4 0.38–0.58

Mrákotín 0.4–1.1 72–157 9–41 91–222 11.2–67.7 0.16–0.48 Číměř/Aalfang 0.5–1.0 96–175 17–54 117–242 21.8–44.2 0.15–0.31

Melechov 0.6–0.8 52–60 3 25–54 6.1–8.9 0.11–0.69

Čeřínek 0.3–0.7 18–114 6–14 93–137 19.9–26.1 0.28–0.32 Zvůle 0.5–0.9 31–88 7–13 88 29.9 0.40 Plechý 0.5–0.7 55–113 9–23 66–118 12.5–20.6 0.13–0.46 Sulzberg 0.5–0.6 130–136 26–35 149–177 27.2–31.8 0.26–0.29

Marginal 2.0–4.1 101–214 7–18 129–199 9.9–16.6 0.56–0.84 Graben granite 1.8–2.3 98–171 10–15 155–238 19.7–30.7 0.58

0.6–1.1 143–291 39–110 207–423 19.9–64.3 0.09–0.31

**ΣREE LaN/YbN Eu/Eu\***

**%**

*DOI: http://dx.doi.org/10.5772/intechopen.93189*

**Suite Variety CaO w.** 

Lipnice/ Steinberg

*Chemical composition of granitic rock of the Moldanubian batholith.*

*Distribution Th and Zr in granitic rocks of the Weinsberg suite.*

Melechov/ Zvůle

*n. a.– not available.*

**Table 1.**


*Geochemistry of Granitic Rocks of the Moldanubian Batholith (Central European Variscides) DOI: http://dx.doi.org/10.5772/intechopen.93189*

#### **Table 1.**

*Geochemistry*

**6**

procedures.

**3. Analytical methods**

**Figure 2.**

*author).*

Rock samples of 2–5 kg in weight were crushed in a jaw crusher and a representative split of these materials was ground in an agate ball mill. For geochemical study of analysed granitoids were used 75 representative rock samples (**Table 1**, **Figures 3**–**7**). Major elements and some trace elements (Ba, Rb, Sr, Zr, Nb, Y, U, and Th) were determined using a Bruker AXS S4 Pioneer X-ray fluorescence spectrometer at the University of Salzburg, Austria, on fused glass discs and pressed rock powder pellets, respectively. The FeO was determined by titration, H2O+

*Schematic geological map of the NW-SE segment of the Moldanubian batholith (after [20] modified by* 

H2O<sup>−</sup> were analyzed gravimetrically in the chemical laboratory of the Institute of Rock Structure and Mechanics, Academy of Sciences of the Czech Republic, Prague.

Microprobe analyses of selected minerals (feldspars and biotite) were performed in polished thin sections using a CAMECA SX-100 microprobe operated in wavelengthdispersive mode at the Institute of Geology, Academy of Sciences of the Czech Republic. The raw analytical data were corrected using the PAP procedure [28]. Operation conditions were accelerating potential of 15–20 kV, beam current of 10–70 nA (measured on

Rare earth elements were quantified by inductive coupled plasma mass spectrometry (ICP-MS) techniques at Activation Laboratories Ltd., Ancaster, Canada, using a Perkin Elmer Sciex ELAN 6100 ICP mass spectrometer, following standard lithium metaborate/tetraborate fusion and acid decomposition sample preparative

and

*Chemical composition of granitic rock of the Moldanubian batholith.*

**Figure 3.** *Distribution Th and Zr in granitic rocks of the Weinsberg suite.*

**Figure 4.** *Chondrite-normalized REE pattern for the Weinsberg suite. Normalizing values are from Boyton [27].*

#### **Figure 5.**

*Distribution of Th and Zr in granitic rocks of the Eisgarn suite.*

a Faraday cup), and a beam diameter of 2 μm. Both synthetic and natural minerals were used as a reference material. Mineral formulae were recalculated using the MinPet 2.02 software [29].

**9**

**4. Results**

**Figure 7.**

**Figure 6.**

**4.1 Petrography**

*Geochemistry of Granitic Rocks of the Moldanubian Batholith (Central European Variscides)*

*Chondrite-normalized REE pattern for the Eisgarn suite. Normalizing values are from Boyton [27].*

The coarse-grained I/S-type granites and granodiorites of the Weinsberg suite are in the Moldanubian batholith represented by four varieties—Weinsberg I, Weisberg II, Schlieren granite, and Srni variety. The subtypes Weinsberg I and II, represented by coarse-grained porphyritic biotite granite to quartz monzodiorite

*Chondrite-normalized REE pattern for the Freistadt suite. Normalizing values are from Boyton [27].*

*DOI: http://dx.doi.org/10.5772/intechopen.93189*

*Geochemistry of Granitic Rocks of the Moldanubian Batholith (Central European Variscides) DOI: http://dx.doi.org/10.5772/intechopen.93189*

**Figure 6.** *Chondrite-normalized REE pattern for the Eisgarn suite. Normalizing values are from Boyton [27].*

**Figure 7.**

*Geochemistry*

**Figure 4.**

**8**

software [29].

**Figure 5.**

a Faraday cup), and a beam diameter of 2 μm. Both synthetic and natural minerals were used as a reference material. Mineral formulae were recalculated using the MinPet 2.02

*Distribution of Th and Zr in granitic rocks of the Eisgarn suite.*

*Chondrite-normalized REE pattern for the Weinsberg suite. Normalizing values are from Boyton [27].*

*Chondrite-normalized REE pattern for the Freistadt suite. Normalizing values are from Boyton [27].*

#### **4. Results**

#### **4.1 Petrography**

The coarse-grained I/S-type granites and granodiorites of the Weinsberg suite are in the Moldanubian batholith represented by four varieties—Weinsberg I, Weisberg II, Schlieren granite, and Srni variety. The subtypes Weinsberg I and II, represented by coarse-grained porphyritic biotite granite to quartz monzodiorite

(Weisberg I) and very coarse-grained porphyritic biotite to muscovite-biotite granite (Weinsberg II), were distinguished based on zircon morphology and minor differences in composition [30, 31]. The Schlieren granite represent predominantly in situ evolved intrusion occurred in the Mühlviertel area (Upper Austria) and attached area of the Bavaria (Germany). The Schlieren granite, however, was originally described as "coarse-grained" gneisses [32]. The Srní variety occurred only in the Vydra and Prášily plutons of the NW-SE segment of the Moldanubian batholith (**Figure 2**) is medium-grained, weakly porphyritic granite to granodiorite. Major components of the Weinsberg granites to quartz monzodiorites are quartz, K-feldspar, plagioclase, biotite and rare amphibole (Schlieren granite), muscovite, or garnet (Srní variety). The accessories include apatite, zircon, ilmenite, titanite, allanite, monazite, and rare xenotime (**Table 2**).

The two-mica granites of the Eisgarn suite are the most abundant granitic rocks in the Moldanubian batholith. Several petrographic varieties in the Eisgarn suite were identified, containing variable texture and biotite to muscovite proportions. In the Czech part of the Moldanubian batholith, the equigranular Mrákotín variety predominates. Similar equigranular two-mica granites occur in the Bavarian part of the Moldanubian batholith (Haidmühle, Theresienreut variety). In the Austrian part of the Moldanubian batholith, the Číměř/Aalfang porphyritic variety with biotite over muscovite predominated. In the Klenov pluton occur the equigranular twomica leucogranites, described as the Deštná variety [33, 34]. In the Melechov and Plechý plutons occur highly porphyritic granites of the Lipnice/Steinberg variety. Major components of the Eisgarn monzogranites are quartz, K-feldspar, plagioclase, biotite, and muscovite. Monazite accessory minerals are represented by apatite, andalusite, ilmenite, zircon, and rare cordierite, sillimanite and xenotime (**Table 3**).

The younger group of highly fractionated S-type two-mica granites of the Melechov/Zvůle suite are composed by coarse-grained two-mica alkali feldspar granites to monzogranites that forms ring-shaped stocks, often with zoned internal structure. There are in the Moldanubian batholith represented by the Melechov, Čeřínek, Zvůle, Plechý plutons, and the Sulzberg granite in the Bärenstein pluton. Major rock-forming minerals of these granites are plagioclase (28–36 vol. %) (An1–23), quartz (27–34 vol. %), K-feldspar (26–31 vol. %),


**11**

**4.2 Geochemistry**

**Table 3.**

*Geochemistry of Granitic Rocks of the Moldanubian Batholith (Central European Variscides)*

Apatite, andalusite, ilmenite, zircon, monazite

Andalusite, apatite, ilmenite, zircon, monazite, cordierite

Apatite, ilmenite, monazite, zircon, rutile, sillimanite

Apatite, ilmenite, monazite, zircon, xenotime

**Accessories Plagioclase Biotite**

An9–25 siderophyllite, Fe/

An9–23 annite–siderophyllite,

An12–25 Annite-siderophyllite, Fe/(Fe + Mg) 0.64–0.74, Al4+ 2.27–2.67, Ti 0.17–0.42

apfu

An13–20 Annite

(Fe + Mg) 0.63–0.72, Al4+ 2.45–2.73, Ti 0.25–0.38 apfu

Fe/(Fe + Mg) 0.64– 0.72, Al4+2.44–2.61, Ti 0.24–0.39 apfu

Fe/(Fe + Mg) 0.59– 0.75, Al4+ 2.10–2.42, Ti 0.22–0.35 apfu

muscovite (3–9 vol. %) and biotite (3–4 vol. %) [annite-siderophyllite, Fe/(Fe + Mg) 0.67–0.77, Al4+ 0.67–0.0.74, Ti 0.16–0.41]. Accessory minerals are represented by

The I/S-type Freistadt biotite granodiorites are medium- to coarse-grained granitic rocks. Major rock-forming minerals of the both main varieties ("central" and "marginal") of the Freistadt suite are quartz, plagioclase, K-feldspar, and biotite. The Graben granite contains also 3 vol. % of muscovite. The accessory minerals in granitic rocks of the Freistadt suite are represented by apatite, ilmenite, zircon, titanite, allanite, and rare xenotime (**Table 4**). The Graben granite is more fraction-

The granites and granodiorites of the Weinsberg suite are subaluminous and weakly peraluminous rocks with A/CNK [mol. Al2O3/(CaO + Na2O + K2O)] of 0.9–1.2. For all varieties of the Weinsberg granite suite are significant high Ba (291–2016 ppm), Sr. (75–680 ppm), Zr (89–652 ppm), and ΣREE (133–491 ppm) concentrations (**Table 1**). The highest concentrations of Ba, Sr, and Zr are significant especially for the Schlieren granite (354–2016 ppm Ba, 196–680 ppm Sr, 133–652 ppm Zr) (**Figure 3**, **Table 1**). For individual varieties of the Weinsberg

The granites of the Eisgarn suite are subaluminous to strongly peraluminous rocks (A/CNK 1.0–1.3) with low CaO concentrations (0.4–1.2 wt. %) (**Table 1**). In the strongly peraluminous varieties, magmatic andalusite, sillimanite, and rarely occurred cordierite are present. In the Mrákotín variety, the peraluminosity is also expressed by widespread dominance of muscovite over biotite. Three main geochemical varieties of two-mica granites could be distinguished by their concentrations of Th on the low-Th (2–7 ppm) Deštná granites, the intermediate Th Mrákotín/ Číměř/Aalfang granites (8–54 ppm), and the high-Th Lipnice/Steinberg granites

apatite, ilmenite, rutile, zircon, monazite, tourmaline, and garnet.

ated granitic rock with relatively high LREE/HREE ratio (20–31).

suite, the partly different fractionation of REE is significant (**Figure 4**).

*DOI: http://dx.doi.org/10.5772/intechopen.93189*

**composition (vol. %)**

22–41, Pl 8–38, Bt 3–16, Ms. 1–8

25–37, Pl 19–37, Bt 6–10, Ms. 2–7

Kfs 21–41, Pl 15–50, Ms. 1–8, Bt 1–5

*Modal composition and mineralogy of granitic rocks of the Eisgarn suite.*

14–42, Pl 10–37, Ms 3–17, Bt 3–11

**Variety Modal** 

Mrákotín Qtz 23–46, Kfs

Číměř/Aalfang Kfs 14–50, Qtz

Lipnice/Steinberg Kfs 23–40, Qtz

Deštná Qtz 28–42,

#### **Table 2.**

*Modal composition and mineralogy of granitic rocks of the Weinsberg suite.*

*Geochemistry of Granitic Rocks of the Moldanubian Batholith (Central European Variscides) DOI: http://dx.doi.org/10.5772/intechopen.93189*


#### **Table 3.**

*Geochemistry*

(Weisberg I) and very coarse-grained porphyritic biotite to muscovite-biotite granite (Weinsberg II), were distinguished based on zircon morphology and minor differences in composition [30, 31]. The Schlieren granite represent predominantly in situ evolved intrusion occurred in the Mühlviertel area (Upper Austria) and attached area of the Bavaria (Germany). The Schlieren granite, however, was originally described as "coarse-grained" gneisses [32]. The Srní variety occurred only in the Vydra and Prášily plutons of the NW-SE segment of the Moldanubian batholith (**Figure 2**) is medium-grained, weakly porphyritic granite to granodiorite. Major components of the Weinsberg granites to quartz monzodiorites are quartz, K-feldspar, plagioclase, biotite and rare amphibole (Schlieren granite), muscovite, or garnet (Srní variety). The accessories include apatite, zircon, ilmenite, titanite, allanite, monazite, and rare xenotime (**Table 2**). The two-mica granites of the Eisgarn suite are the most abundant granitic rocks in the Moldanubian batholith. Several petrographic varieties in the Eisgarn suite were identified, containing variable texture and biotite to muscovite proportions. In the Czech part of the Moldanubian batholith, the equigranular Mrákotín variety predominates. Similar equigranular two-mica granites occur in the Bavarian part of the Moldanubian batholith (Haidmühle, Theresienreut variety). In the Austrian part of the Moldanubian batholith, the Číměř/Aalfang porphyritic variety with biotite over muscovite predominated. In the Klenov pluton occur the equigranular twomica leucogranites, described as the Deštná variety [33, 34]. In the Melechov and Plechý plutons occur highly porphyritic granites of the Lipnice/Steinberg variety. Major components of the Eisgarn monzogranites are quartz, K-feldspar, plagioclase, biotite, and muscovite. Monazite accessory minerals are represented by apatite, andalusite, ilmenite, zircon, and rare cordierite, sillimanite and xenotime (**Table 3**). The younger group of highly fractionated S-type two-mica granites of the Melechov/Zvůle suite are composed by coarse-grained two-mica alkali feldspar granites to monzogranites that forms ring-shaped stocks, often with zoned internal structure. There are in the Moldanubian batholith represented by the Melechov, Čeřínek, Zvůle, Plechý plutons, and the Sulzberg granite in the Bärenstein pluton. Major rock-forming minerals of these granites are plagioclase (28–36 vol. %) (An1–23), quartz (27–34 vol. %), K-feldspar (26–31 vol. %),

**10**

**Table 2.**

**Variety Modal** 

Weinsberg II

Schlieren granite

Weinsberg I Qtz 16–43, Kfs

**composition (vol. %)**

12–54, Pl 11–44, Bt 6–27

Qtz 24–30, Kfs 22–33, Pl 23–37, Bt

Pl 32–50, Kfs 7–37, Qtz 18–34, Bt 6–32, Amp 0–3

Kfs 7–41, Bt 4–27, Ms 0–6, Gt 0–3

*Modal composition and mineralogy of granitic rocks of the Weinsberg suite.*

7–15

Srní Pl 19–53, Pl 19–53,

**Accessories Plagioclase Biotite**

An15–42 Annite, Fe/(Fe+ Mg)

An24–41 Annite, Fe/(Fe+ Mg)

An20–40 Annite, Fe/(Fe+ Mg)

apfu

An9–31 Annite-siderophyllite,

0.60–0.67, Al4+2.05–2.39, Ti 0.23–0.45 apfu

0.79–0.81, Al4+ 2.43–2.47, Ti 0.34–0.42 apfu

Fe/(Fe+ Mg) 0.64–0.81, Al4+ 2.24–2.57, Ti 0.26–0.42 apfu

0.0.53–0.55, Al4+ 2.10–2.13, Ti 0.23–0.42

Apatite, zircon, ilmenite, titanite, monazite, allanite

Apatite, zircon, ilmenite, monazite

Apatite, zircon, titanite, ilmenite, magnetite, allanite

Apatite, zircon, ilmenite, monazite, xenotime

*Modal composition and mineralogy of granitic rocks of the Eisgarn suite.*

muscovite (3–9 vol. %) and biotite (3–4 vol. %) [annite-siderophyllite, Fe/(Fe + Mg) 0.67–0.77, Al4+ 0.67–0.0.74, Ti 0.16–0.41]. Accessory minerals are represented by apatite, ilmenite, rutile, zircon, monazite, tourmaline, and garnet.

The I/S-type Freistadt biotite granodiorites are medium- to coarse-grained granitic rocks. Major rock-forming minerals of the both main varieties ("central" and "marginal") of the Freistadt suite are quartz, plagioclase, K-feldspar, and biotite. The Graben granite contains also 3 vol. % of muscovite. The accessory minerals in granitic rocks of the Freistadt suite are represented by apatite, ilmenite, zircon, titanite, allanite, and rare xenotime (**Table 4**). The Graben granite is more fractionated granitic rock with relatively high LREE/HREE ratio (20–31).

#### **4.2 Geochemistry**

The granites and granodiorites of the Weinsberg suite are subaluminous and weakly peraluminous rocks with A/CNK [mol. Al2O3/(CaO + Na2O + K2O)] of 0.9–1.2. For all varieties of the Weinsberg granite suite are significant high Ba (291–2016 ppm), Sr. (75–680 ppm), Zr (89–652 ppm), and ΣREE (133–491 ppm) concentrations (**Table 1**). The highest concentrations of Ba, Sr, and Zr are significant especially for the Schlieren granite (354–2016 ppm Ba, 196–680 ppm Sr, 133–652 ppm Zr) (**Figure 3**, **Table 1**). For individual varieties of the Weinsberg suite, the partly different fractionation of REE is significant (**Figure 4**).

The granites of the Eisgarn suite are subaluminous to strongly peraluminous rocks (A/CNK 1.0–1.3) with low CaO concentrations (0.4–1.2 wt. %) (**Table 1**). In the strongly peraluminous varieties, magmatic andalusite, sillimanite, and rarely occurred cordierite are present. In the Mrákotín variety, the peraluminosity is also expressed by widespread dominance of muscovite over biotite. Three main geochemical varieties of two-mica granites could be distinguished by their concentrations of Th on the low-Th (2–7 ppm) Deštná granites, the intermediate Th Mrákotín/ Číměř/Aalfang granites (8–54 ppm), and the high-Th Lipnice/Steinberg granites


#### **Table 4.**

*Modal composition and mineralogy of granodiorites and granites of the Freistadt suite.*

(39–110 ppm) (**Table 1**, **Figure 5**). The highest ΣREE was found in the Lipnice/ Steinberg granite variety (207–242 ppm), whereas the lowest ΣREE is for the Deštná granites significant (33–69 ppm). The highest LREE/HREE ratio is for the Lipnice/ Steinberg variety significant (**Figure 6**).

The granites of the Melechov/Zvůle granite suite are peraluminous rocks (A/CNK 1.1–1.3) with low CaO concentrations (0.3–0.9 wt. %) (**Table 1**). The individual varieties of these granites could be distinguished especially by their concentrations of Zr and Th. The highest concentrations of both elements are significant for the Plechý (55–113 ppm Zr, 9–23 ppm Th) and Sulzberg (130–136 ppm Zr, 26–35 ppm Th) granites. The lowest concentrations of the both elements occur in the Stvořidla granites, which form the central stock in the Melechov pluton (36–67 ppm Zr, 2.8–2.9 ppm Th). These granites also have the lowest concentrations of ΣREE (27–35 ppm) and the lowest LREE/HREE ratio (3.2–8.6). In the opposite, the highest content of ΣREE (149–177 ppm) and the highest LREE/ HREE ratio (27–32) are for the Sulzberg granites significant.

The granites and granodiorites of the Freistadt suite are subaluminous rocks (A/CNK = 1.0–1.1) with partly elevated CaO concentrations (1.8–4.1 wt. %). The central and marginal granodiorites of this suite are enriched in Ba (616–1017 ppm) and Sr (253–471 ppm). Their total concentrations of REE in granites and granodiorites of the Freistadt suite are 129–238 ppm and the central and marginal granodiorites display relatively low LREE/HREE ratio (9–21) with moderate negative Eu anomaly (Eu/Eu\* = 0.56–0.84) (**Table 1**, **Figure 7**).

#### **5. Discussion**

In the past, the orig

in and fractionation of granitic rocks of the Moldanubian batholith was discussed by geochemical modelling based on trace-element fractionation [6, 18, 31, 35, 36] and experimental study of biotite stability [34]. According to these studies, granitic rocks of the Moldanubian batholith could originated by LP-HT partial melting of various metasediments and/or by melting of a mixture of metasediments and amphibolites [6, 18, 31, 36]. According to the majority of these studies, the granitic rocks of the individual magmatic suites occurred in the Moldanubian batholith were also differently fractionated [35, 36]. The fractionation of these magmatic suites

**13**

**6. Conclusion**

*Geochemistry of Granitic Rocks of the Moldanubian Batholith (Central European Variscides)*

could be well documented by distribution some trace elements (e.g., Ba, Sr, Th, Zr,

For distinguishing, source rock series (greywackes vs. pelites) could be used CaO/Na2O and Al2O3/TiO2 ratios [37]. According to this study, discussed in detail by René et al. [34] and René [18], the granitic rocks of the Eisgarn suite originated by partial melting of metapelites, whereas granites and granodiorites of the Weinsberg and Freistadt suites originated by partial melting of a metagreywackes-

The estimation of melting temperatures of granitic melts is usually based on saturation thermometers based on melting of zircon and monazite [38–40]. According to zircon saturation, thermometry granitic rocks are usually divided on the hot and cold granites [41]. The most detailed study of all problems connected with the use of zircon thermometry was published by Siégel et al. [42] and Clemens et al. [43]. For all granitic rocks from the Moldanubian batholith, the TZrnsat was calculated according to the revisited formula published by Boehnke et al. [39] and TMnzsat according to the model of Montel [40]. The highest saturation temperatures from both models were found for granitic rocks of the Weinsberg suite (681–900°C) and for the Zr- and Th-enriched Lipnice/Steinberg granites of the Eisgarn suite °C (760–910°C). The lowest saturation temperatures were found for some two-mica granites of the Eisgarn suite, especially for the Zr- and Th-depleted Deštná granites (628–740°C). The saturation temperatures for the Mrákotín granites varied between 682 and 859°C. However, the crystallisation temperature derived from experimental melting of biotite for the Mrákotín granite is 830–850°C [34]. It is also interested that in all these cases that the TMnzsat temperatures are usually partly higher that the TZrnsat temperatures. These differences could be explained by restitic (inherited) monazite crystals from original metasediments. On the other hand, during detailed study of zircon crystals from granites of the Eisgarn suite in rare cases, inherited

zircon cores overgrowth by younger magmatic zircon were found [44].

shear zones that are later multiply reactivated [13, 15].

Partly controversial are sources of heating, which were used for the generation of magmatic rocks of the Moldanubian batholith. According to Velmer and Wedepohl [6], the main heating source of the Moldanubian crust was intrusion of tholeiitic rocks during underplating of an upper crust. However, Gerdes et al. [8] proposed as a main heat source the contribution of internal radiogenic heat production within the thickened upper crust. Some other source of heating needed for generation of granitic rocks in the NW-SE segment of the Moldanubian batholith, together with LP-HT metamorphism rock series southern of the Pfahl zone, was a late Variscan delamination of upper mantle [10, 45]. Recent structural studies that granite plutons in the NW-SE segment of the Moldanubian batholith were emplaced at a shallow level into previously exhumed upper crust during dextral strike-slip

Granitic rocks of the Moldanubian batholith are represented by four magmatic

suites. The biotite granites of the Weinsberg suite are subaluminous to weakly peraluminous granites enriched especially in Ba, Sr, and Zr. The two-mica granites of the Eisgarn suite are represented by the low-Th Deštná granites, the intermediate-Th Mrákotín, Číměř/Aalfang granites, and the high-Th Lipnice/Steinberg granites. The highly fractionated alkali feldspar and two-mica granites of the Melechov/ Zvůle suite are depleted in Ba, Zr, and Th. The granites to granodiorites of the Freistadt suite are of Ba- and Sr-enriched granitic rocks. The granitic rocks of the individual magmatic suites occurred in the Moldanubian batholith were variable

*DOI: http://dx.doi.org/10.5772/intechopen.93189*

REE) (**Figures 3**–**7**).

metabasalt mixture.

*Geochemistry of Granitic Rocks of the Moldanubian Batholith (Central European Variscides) DOI: http://dx.doi.org/10.5772/intechopen.93189*

could be well documented by distribution some trace elements (e.g., Ba, Sr, Th, Zr, REE) (**Figures 3**–**7**).

For distinguishing, source rock series (greywackes vs. pelites) could be used CaO/Na2O and Al2O3/TiO2 ratios [37]. According to this study, discussed in detail by René et al. [34] and René [18], the granitic rocks of the Eisgarn suite originated by partial melting of metapelites, whereas granites and granodiorites of the Weinsberg and Freistadt suites originated by partial melting of a metagreywackesmetabasalt mixture.

The estimation of melting temperatures of granitic melts is usually based on saturation thermometers based on melting of zircon and monazite [38–40]. According to zircon saturation, thermometry granitic rocks are usually divided on the hot and cold granites [41]. The most detailed study of all problems connected with the use of zircon thermometry was published by Siégel et al. [42] and Clemens et al. [43]. For all granitic rocks from the Moldanubian batholith, the TZrnsat was calculated according to the revisited formula published by Boehnke et al. [39] and TMnzsat according to the model of Montel [40]. The highest saturation temperatures from both models were found for granitic rocks of the Weinsberg suite (681–900°C) and for the Zr- and Th-enriched Lipnice/Steinberg granites of the Eisgarn suite °C (760–910°C). The lowest saturation temperatures were found for some two-mica granites of the Eisgarn suite, especially for the Zr- and Th-depleted Deštná granites (628–740°C). The saturation temperatures for the Mrákotín granites varied between 682 and 859°C. However, the crystallisation temperature derived from experimental melting of biotite for the Mrákotín granite is 830–850°C [34]. It is also interested that in all these cases that the TMnzsat temperatures are usually partly higher that the TZrnsat temperatures. These differences could be explained by restitic (inherited) monazite crystals from original metasediments. On the other hand, during detailed study of zircon crystals from granites of the Eisgarn suite in rare cases, inherited zircon cores overgrowth by younger magmatic zircon were found [44].

Partly controversial are sources of heating, which were used for the generation of magmatic rocks of the Moldanubian batholith. According to Velmer and Wedepohl [6], the main heating source of the Moldanubian crust was intrusion of tholeiitic rocks during underplating of an upper crust. However, Gerdes et al. [8] proposed as a main heat source the contribution of internal radiogenic heat production within the thickened upper crust. Some other source of heating needed for generation of granitic rocks in the NW-SE segment of the Moldanubian batholith, together with LP-HT metamorphism rock series southern of the Pfahl zone, was a late Variscan delamination of upper mantle [10, 45]. Recent structural studies that granite plutons in the NW-SE segment of the Moldanubian batholith were emplaced at a shallow level into previously exhumed upper crust during dextral strike-slip shear zones that are later multiply reactivated [13, 15].

#### **6. Conclusion**

Granitic rocks of the Moldanubian batholith are represented by four magmatic suites. The biotite granites of the Weinsberg suite are subaluminous to weakly peraluminous granites enriched especially in Ba, Sr, and Zr. The two-mica granites of the Eisgarn suite are represented by the low-Th Deštná granites, the intermediate-Th Mrákotín, Číměř/Aalfang granites, and the high-Th Lipnice/Steinberg granites. The highly fractionated alkali feldspar and two-mica granites of the Melechov/ Zvůle suite are depleted in Ba, Zr, and Th. The granites to granodiorites of the Freistadt suite are of Ba- and Sr-enriched granitic rocks. The granitic rocks of the individual magmatic suites occurred in the Moldanubian batholith were variable

*Geochemistry*

Freistadt central

Freistadt marginal

Graben granite

**Table 4.**

**Variety Modal composition (vol. %)**

Ms 0–2

Qtz 23–29, Pl 34–49, Kfs 13–25, Bt 9–14,

Qtz 12–32, Pl 32–68, Kfs 3–27, Bt 6–17, Ms 0–1

Qtz 29–31, Pl 33–40, Kfs 19–25, Bt 5–9, Ms 2–6

(39–110 ppm) (**Table 1**, **Figure 5**). The highest ΣREE was found in the Lipnice/ Steinberg granite variety (207–242 ppm), whereas the lowest ΣREE is for the Deštná granites significant (33–69 ppm). The highest LREE/HREE ratio is for the Lipnice/

*Modal composition and mineralogy of granodiorites and granites of the Freistadt suite.*

Apatite, zircon, ilmenite, monazite, titanite, xenotime

Apatite, zircon, ilmenite, titanite, monazite, allanite

Apatite, zircon, ilmenite, monazite

**Accessories Plagioclase Biotite**

An20–22 Annite

An25–37 Annite

An23–26 Annite

Fe/(Fe + Mg) 0.58– 0.59, Al4+ 2.20–2.24, Ti 0.34–0.47 apfu

Fe/(Fe + Mg) 0.44– 0.62, Al4+2.09–2.28, Ti 0.30–0.50 apfu

Fe/(Fe + Mg) 0.66–0.69, Al4+ 2.33–2.41, Ti 0.31–0.41

apfu

The granites of the Melechov/Zvůle granite suite are peraluminous rocks (A/CNK 1.1–1.3) with low CaO concentrations (0.3–0.9 wt. %) (**Table 1**). The individual varieties of these granites could be distinguished especially by their concentrations of Zr and Th. The highest concentrations of both elements are significant for the Plechý (55–113 ppm Zr, 9–23 ppm Th) and Sulzberg (130–136 ppm Zr, 26–35 ppm Th) granites. The lowest concentrations of the both elements occur in the Stvořidla granites, which form the central stock in the Melechov pluton (36–67 ppm Zr, 2.8–2.9 ppm Th). These granites also have the lowest concentrations of ΣREE (27–35 ppm) and the lowest LREE/HREE ratio (3.2–8.6). In the opposite, the highest content of ΣREE (149–177 ppm) and the highest LREE/

The granites and granodiorites of the Freistadt suite are subaluminous rocks (A/CNK = 1.0–1.1) with partly elevated CaO concentrations (1.8–4.1 wt. %). The central and marginal granodiorites of this suite are enriched in Ba (616–1017 ppm) and Sr (253–471 ppm). Their total concentrations of REE in granites and granodiorites of the Freistadt suite are 129–238 ppm and the central and marginal granodiorites display relatively low LREE/HREE ratio (9–21) with moderate negative Eu

in and fractionation of granitic rocks of the Moldanubian batholith was discussed by geochemical modelling based on trace-element fractionation [6, 18, 31, 35, 36] and experimental study of biotite stability [34]. According to these studies, granitic rocks of the Moldanubian batholith could originated by LP-HT partial melting of various metasediments and/or by melting of a mixture of metasediments and amphibolites [6, 18, 31, 36]. According to the majority of these studies, the granitic rocks of the individual magmatic suites occurred in the Moldanubian batholith were also differently fractionated [35, 36]. The fractionation of these magmatic suites

HREE ratio (27–32) are for the Sulzberg granites significant.

anomaly (Eu/Eu\* = 0.56–0.84) (**Table 1**, **Figure 7**).

Steinberg variety significant (**Figure 6**).

**12**

**5. Discussion**

In the past, the orig

fractionated. The fractionation of these magmatic suites is documented by distribution some trace elements, especially by the Ba, Sr, Th, Zr, and REE. The granitic rocks of the Eisgarn suite originated by partial melting of metapelites, whereas granites and granodiorites of the Weinsberg and Freistadt suites originated by partial melting of a metagreywackes-metabasalt mixture. The estimation of melting temperatures of granitic melts for all magmatic suites of the Moldanubian batholith, based on zircon and monazite saturation thermometers, show that the highest temperatures from both models were found for granitic rocks of the Weinsberg suite and for Zr- and Th-enriched Lipnice/Steinberg granites from the Eisgarn suite (681–910°C). The partial differences between both saturation thermometers could be explained especially by restitic (inherited) zircon and monazite occurred in investigated granitic rocks.

### **Acknowledgements**

Thanks are extended to the support of the long-term conceptual development research organization RVO 67985891 and the project of Ministry of Education, Youth and Sports (ME10083). The author is also grateful to Z. Korbelová from the Geological Institute of the Academy of Sciences of the Czech Republic for her technical assistance by using electron microprobe analyses of selected minerals (plagioclase, biotite). I am grateful to anonymous reviewer for numerous comments and recommendations that helped to improve this paper.

### **Conflict of interest**

The author declares no conflict of interests.

### **Author details**

Miloš René

Institute of Rock Structure and Mechanics, v.v.i., Academy of Sciences of the Czech Republic, Prague, Czech Republic

\*Address all correspondence to: rene@irsm.cas.cz

© 2020 The Author(s). Licensee IntechOpen. This chapter is distributed under the terms of the Creative Commons Attribution License (http://creativecommons.org/licenses/ by/3.0), which permits unrestricted use, distribution, and reproduction in any medium, provided the original work is properly cited.

**15**

BF00310608

*Geochemistry of Granitic Rocks of the Moldanubian Batholith (Central European Variscides)*

and Petrology. 1997;**61**:67-96. DOI:

[8] Gerdes A, Wörner G, Henk A. Postcollisional granite generation and HT/LP metamorphism by radiogenic heating: The Variscan south bohemian batholith. Journal of the Geological Society of London. 2000;**157**:577-587.

DOI: 10.1144/jgs.157.3.577

[9] Breiter K. Geochemical

2010;**65**:19-25

10.1144/SP405.9

classification of Variscan granitoids in the Moldanubicum (Czech Republic, Austria). Abhandlungen der Geologischen Bundesanstalt.

[10] Žák J, Verner K, Janoušek V, Holub FV, Kachlík V, Finger F, et al. A plate-kinematic model for the assembly of the bohemian massif constrained by relationships around granitoid plutons. Geological Society of London, Special Publication. 2014;**405**:169-196. DOI:

[11] Siebel W, Shang CK, Reiter E, Rohrmüller J, Breiter K. Two distinctive granite suites in the SW bohemian massif and their record of emplacement: Constraints from geochemistry and zircon 207Pb/208Pb chronology. Journal of Petrology. 2008;**49**:1853-1872. DOI:

10.1093/petrology/egn049

10.1007/s00531-007-0285-9

shear zones in the southern bohemian massif (Austria):

[13] Brandmayr M, Dallmeyer RD, Handler R, Wallbrecher E. Conjugate

[12] Verner K, Žák J, Pertoldová J, Šrámek J, Trubač J, Týcová P. Magmatic history and geophysical signature of a post-collisional intrusive center emplaced near a crustal-scale shear zone: The Plechý granite pluton (Moldanubian batholith, bohemian massif). International Journal of Earth Sciences. 2009;**98**:517-532. DOI:

10.1007/BF01172478

*DOI: http://dx.doi.org/10.5772/intechopen.93189*

[1] Williamson BJ, Shaw A, Downes H, Thirlwall MF. Geochemical constraints

on the genesis of Hercynian two-mica leucogranites from the Massif Central, France. Chemical Geology. 1996;**127**:25-42. DOI: 10.1016/0009-2541(95)00105-0

**References**

[2] Clemens JD. S-type granitic magmas—Petrogenetic issues, models and evidence. Earth-Science Reviews. 2003;**61**:1-18. DOI: 10.1016/

[3] Chappell BW, Hine T. The Cornubian batholith: An example of magmatic fractionation on a crustal scale. Resource Geology. 2006;**56**:203- 244. DOI: 10.1111/j.1751-3928.2006.

S0012-8252(02)00107-1

[4] Janoušek V, Moyen JF, Martin H, Erban V, Farrow C. Geochemical modelling of igneous processes—Principles and recipes in R language. In: Bringing the Power of R to a Geochemical Community. 1st ed. Berlin, Heidelberg: Springer

Geochemistry. p. 346. DOI: 10.1007/978-3-662-46792-3

[5] Liew TC, Finger F, Höck V. The Moldanubian granitoid plutons of Austria: Chemical and isotopic studies bearing on their environmental setting. Chemical Geology. 1989;**76**:41-55. DOI:

10.1016/0009-2541(89)90126-5

[6] Vellmer C, Wedepohl KH. Geochemical characterization and origin of granitoids from the south bohemian batholith in Lower Austria. Contributions to Mineralogy and Petrology. 1994;**118**:13-32. DOI: 10.1007/

[7] Finger F, Roberts MP, Haunschmid B, Schermaier A, Steyer HP. Variscan granitoids of Central Europe: Their typology, potential sources and tectonothermal relations. Mineralogy

tb00281.x

*Geochemistry of Granitic Rocks of the Moldanubian Batholith (Central European Variscides) DOI: http://dx.doi.org/10.5772/intechopen.93189*

#### **References**

*Geochemistry*

investigated granitic rocks.

**Acknowledgements**

**Conflict of interest**

**14**

**Author details**

Republic, Prague, Czech Republic

\*Address all correspondence to: rene@irsm.cas.cz

provided the original work is properly cited.

and recommendations that helped to improve this paper.

The author declares no conflict of interests.

Institute of Rock Structure and Mechanics, v.v.i., Academy of Sciences of the Czech

© 2020 The Author(s). Licensee IntechOpen. This chapter is distributed under the terms of the Creative Commons Attribution License (http://creativecommons.org/licenses/ by/3.0), which permits unrestricted use, distribution, and reproduction in any medium,

fractionated. The fractionation of these magmatic suites is documented by distribution some trace elements, especially by the Ba, Sr, Th, Zr, and REE. The granitic rocks of the Eisgarn suite originated by partial melting of metapelites, whereas granites and granodiorites of the Weinsberg and Freistadt suites originated by partial melting of a metagreywackes-metabasalt mixture. The estimation of melting temperatures of granitic melts for all magmatic suites of the Moldanubian batholith, based on zircon and monazite saturation thermometers, show that the highest temperatures from both models were found for granitic rocks of the Weinsberg suite and for Zr- and Th-enriched Lipnice/Steinberg granites from the Eisgarn suite (681–910°C). The partial differences between both saturation thermometers could be explained especially by restitic (inherited) zircon and monazite occurred in

Thanks are extended to the support of the long-term conceptual development research organization RVO 67985891 and the project of Ministry of Education, Youth and Sports (ME10083). The author is also grateful to Z. Korbelová from the Geological Institute of the Academy of Sciences of the Czech Republic for her technical assistance by using electron microprobe analyses of selected minerals (plagioclase, biotite). I am grateful to anonymous reviewer for numerous comments

Miloš René

[1] Williamson BJ, Shaw A, Downes H, Thirlwall MF. Geochemical constraints on the genesis of Hercynian two-mica leucogranites from the Massif Central, France. Chemical Geology. 1996;**127**:25-42. DOI: 10.1016/0009-2541(95)00105-0

[2] Clemens JD. S-type granitic magmas—Petrogenetic issues, models and evidence. Earth-Science Reviews. 2003;**61**:1-18. DOI: 10.1016/ S0012-8252(02)00107-1

[3] Chappell BW, Hine T. The Cornubian batholith: An example of magmatic fractionation on a crustal scale. Resource Geology. 2006;**56**:203- 244. DOI: 10.1111/j.1751-3928.2006. tb00281.x

[4] Janoušek V, Moyen JF, Martin H, Erban V, Farrow C. Geochemical modelling of igneous processes—Principles and recipes in R language. In: Bringing the Power of R to a Geochemical Community. 1st ed. Berlin, Heidelberg: Springer Geochemistry. p. 346. DOI: 10.1007/978-3-662-46792-3

[5] Liew TC, Finger F, Höck V. The Moldanubian granitoid plutons of Austria: Chemical and isotopic studies bearing on their environmental setting. Chemical Geology. 1989;**76**:41-55. DOI: 10.1016/0009-2541(89)90126-5

[6] Vellmer C, Wedepohl KH. Geochemical characterization and origin of granitoids from the south bohemian batholith in Lower Austria. Contributions to Mineralogy and Petrology. 1994;**118**:13-32. DOI: 10.1007/ BF00310608

[7] Finger F, Roberts MP, Haunschmid B, Schermaier A, Steyer HP. Variscan granitoids of Central Europe: Their typology, potential sources and tectonothermal relations. Mineralogy

and Petrology. 1997;**61**:67-96. DOI: 10.1007/BF01172478

[8] Gerdes A, Wörner G, Henk A. Postcollisional granite generation and HT/LP metamorphism by radiogenic heating: The Variscan south bohemian batholith. Journal of the Geological Society of London. 2000;**157**:577-587. DOI: 10.1144/jgs.157.3.577

[9] Breiter K. Geochemical classification of Variscan granitoids in the Moldanubicum (Czech Republic, Austria). Abhandlungen der Geologischen Bundesanstalt. 2010;**65**:19-25

[10] Žák J, Verner K, Janoušek V, Holub FV, Kachlík V, Finger F, et al. A plate-kinematic model for the assembly of the bohemian massif constrained by relationships around granitoid plutons. Geological Society of London, Special Publication. 2014;**405**:169-196. DOI: 10.1144/SP405.9

[11] Siebel W, Shang CK, Reiter E, Rohrmüller J, Breiter K. Two distinctive granite suites in the SW bohemian massif and their record of emplacement: Constraints from geochemistry and zircon 207Pb/208Pb chronology. Journal of Petrology. 2008;**49**:1853-1872. DOI: 10.1093/petrology/egn049

[12] Verner K, Žák J, Pertoldová J, Šrámek J, Trubač J, Týcová P. Magmatic history and geophysical signature of a post-collisional intrusive center emplaced near a crustal-scale shear zone: The Plechý granite pluton (Moldanubian batholith, bohemian massif). International Journal of Earth Sciences. 2009;**98**:517-532. DOI: 10.1007/s00531-007-0285-9

[13] Brandmayr M, Dallmeyer RD, Handler R, Wallbrecher E. Conjugate shear zones in the southern bohemian massif (Austria):

Implications for Variscan and alpine tectonothermal activity. Tectonophysics. 1995;**248**:97-116. DOI: 10.1016/0040-1951(95)00003-6

[14] Büttner SH. The geometric evolution of structures in granite during continuous deformation from magmatic to solid-state conditions: An example from the central European Variscan belt. American Mineralogist. 1999;**84**:1781-1792

[15] Büttner SH. Late Variscan stressfield rotation initiating escape tectonics in the south-western bohemian massif: A far field response to late-orogenic extension. Journal of Geosciences. 2007;**52**:29-43. DOI: 10.3190/j. geosci.004

[16] Žák J, Verner K, Faryad W, Chlupáčová M, Veselovský F. The generation of voluminous S-type granites in the Moldanubian unit, bohemian massif, by rapid isothermal exhumation of the metapelitic middle crust. Lithos. 2011;**121**:25-40. DOI: 10.1016/j.lithos.2010-10.002

[17] Žák J, Verner K, Ježek J, Trubač J. Complex mid-crustal flow within a growing granite-migmatite dome: An example from the Variscan belt illustrated by the anisotropy of magnetic susceptibility and fabric modelling. Geological Journal. 2019;**54**:3681-3699. DOI: 10.1002/gj.3335

[18] René M. Source compositions and melting temperatures of the main granitic suites from the Moldanubian batholith. Journal of Geosciences. 2016;**61**:355-370. DOI: 10.3190/ jgeosci.223

[19] Fuchs G. Exkursion III/4: Kristallin Mühlviertel und Sauwald, südliche Böhmische Masse. Mitteilungen der Geologische Gesellschaft. 1964;**57**:281-289

[20] Klomínský J, Jarchovský T, Rajpoot GS. Atlas of Plutonic Rocks and Orthogneisses in the Bohemian Massif. 2. Moldanubicum. 1st ed. Prague: Czech Geological Survey; 2010. p. 200

[21] Klob H. Freistädter Granodiorit im österreichischen Moldanubikum. Verhandlungen der Geologische Bundesanstalt. 1971;**1**:98-142

[22] Friedl G. Geologischpetrographische Untersuchungen in der Gegend nordöstlich von Freistadt (Oberösterreich) mit besonderer Berücksichtigung des "Grabengranits" [thesis]. Salzburg: University of Salzburg; 1990

[23] Klötzli US, Koller F, Scharbert S, Höck V. Cadomian lower-crustal contributions to Variscan Granit Petrogenesis (south bohemian pluton, Austria): Constraints from zircon typology and geochemistry, whole-rock, and feldspar Pb-Sr isotope systematics. Journal of Petrology. 2001;**42**:1621-1642. DOI: 10.1093/petrology/42.9.1621

[24] Finger F, Gerdes A, Verner K, Žák J. Resolving the growth history of the South Bohemian Batholith by means of high-precision ID-TIMS U-Pb zircon and monazite dating. In: Proceedings of the 3rd Workshop on Orogenic Processes in the Bohemian Massif; 15-17 June 2018; Presseck; 2018. pp. 13-14

[25] Gerdes A, Friedl G, Parrish RR, von Quadt A, Finger F. U-Pb-Datierungen (TIMS, SHRIMP und LA-MC-ICP-MS) an Zirkonen und Monaziten Südböhmischer Granitoide. Erlangen Geologische Abhandlungen. 2002;**Sonderband 4**:30-32

[26] Gerdes A, Friedl G, Parrish RR, Finger F. High-resolution geochronology of Variscan granite emplacement—The south bohemian batholith. Journal of the Czech Geological Society. 2003;**48**:53-54

**17**

*Geochemistry of Granitic Rocks of the Moldanubian Batholith (Central European Variscides)*

[35] Finger F, Clemens J. Migmatization and "secondary" granitic magmas: Effects of emplacement and

crystallization of "primary" granitoids in southern Bohemian Massif, Austria. Contributions to Mineralogy and Petrology. 1995;**120**:311-326. DOI:

[36] Matějka D, Janoušek V. Wholerock geochemistry and petrogenesis of granites from the northern part of the Moldanubian Batholith (Czech Republic). Acta Universitatis Carolineae, Geology. 1998;**42**:73-79

[37] Sylvester PJ. Post-collisional strongly peraluminous granites. Lithos. 1998;**45**:29-44. DOI: 10.1016/

[38] Watson EB, Harrison TM. Zircon saturation revisited: Temperature and composition effects in a variety of crustal magma types. Earth and Planetary Science Letters. 1983;**64**:295-304. DOI: 10.1016/0012-821X(83)90211-X

[39] Boehnke P, Watson EB, Trail D, Harrison TM, Schmitt AK. Zircon saturation re-revisited. Chemical Geology. 2013;**351**:324-334. DOI: 10.1016/j.chemgeo.2013.05.028

[40] Montel JM. A model for monazite/ melt equilibrium and applications to the generation of granitic magmas. Chemical geology. 1993;**110**:127-146

[41] Miller CF. Hot and cold granites? Implications of zircon saturation temperatures and preservation of inheritance. Geology. 2003;**31**:529-532. DOI: 10.1130/0091-7613(2003)031

[42] Siégel C, Bryan SE, Allen CM, Gust DA. Use and abuse of zircon-based thermometers: A critical review and a recommended approach to identify atecrystic zircon. Earth-Science Reviews. 2018;**176**:87-116. DOI: 10.1016/j.earscirev.2017.08.011

S0024-4937(98)00024-3

10.1007/BF00306510

*DOI: http://dx.doi.org/10.5772/intechopen.93189*

[28] Pouchou JL, Pichoir F. PAP (φ-ρ-Z) procedure for improved quantitative microanalysis. In: Armstrong JT, editor. Microbeam Analysis. San Francisco: San Francisco Press; 1985.

[29] Richard R. MinPet: mineralogical and petrological data processing system, version 2.02. Québec, Canada: MinPet

[30] Stöbich DM. Trachstudien an den akzessorischen Zirkonen des Weinsberger Granits im östlichen Mühlviertel und westlichen Waldviertel

[thesis]. Salzburg: University of

during anataxis, ascent and/or emplacement? Constraints from the Variscan Weinsberg granites. Terra Nova. 2001;**13**:305-312. DOI: 10.1046/j.1365-3121.2001.00365.x

[32] Fuchs G. Zur Altersgliederung des Moldanubikums Oberösterreichs. Vienna: Verhandlungen der Geologische

Bundesanstalt; 1962. pp. 96-117

[33] René M, Matějka D, Nosek T. Geochemical constraints on the origin of a distinct type of two-mica granites (Deštná–Lásenice type) in the Moldanubian batholith (Czech Republic). Acta Montana, Geodynamics. Series A. 2003;**23**:59-76

[34] René M, Holtz F, Luo C,

in peraluminous granitic melts: Compositional dependence and application to the generation of twomica granites in the South Bohemian batholith (Bohemian Massif, Czech Republic). Lithos. 2008;**102**:538-553. DOI: 10.1016/j.lithos.2007.07.022

Beermann O, Stelling J. Biotite stability

[31] Gerdes A. Magma homogenisation

Geological Software; 1995

pp. 104-106

Salzburg; 1992

studies. In: Henderson P, editor. Rare Earth Element Geochemistry. 1st ed. Amsterdam: Elsevier; 1984. pp. 63-114

[27] Boyton WV. Geochemistry of the rare earth elements: Meteorite *Geochemistry of Granitic Rocks of the Moldanubian Batholith (Central European Variscides) DOI: http://dx.doi.org/10.5772/intechopen.93189*

studies. In: Henderson P, editor. Rare Earth Element Geochemistry. 1st ed. Amsterdam: Elsevier; 1984. pp. 63-114

*Geochemistry*

Implications for Variscan and alpine tectonothermal activity.

[14] Büttner SH. The geometric evolution of structures in granite during continuous deformation from magmatic to solid-state conditions: An example from the central European Variscan belt. American Mineralogist.

[15] Büttner SH. Late Variscan stressfield rotation initiating escape tectonics in the south-western bohemian massif: A far field response to late-orogenic extension. Journal of Geosciences. 2007;**52**:29-43. DOI: 10.3190/j.

[16] Žák J, Verner K, Faryad W, Chlupáčová M, Veselovský F. The generation of voluminous S-type granites in the Moldanubian unit, bohemian massif, by rapid isothermal exhumation of the metapelitic middle crust. Lithos. 2011;**121**:25-40. DOI: 10.1016/j.lithos.2010-10.002

[17] Žák J, Verner K, Ježek J, Trubač J. Complex mid-crustal flow within a growing granite-migmatite dome: An example from the Variscan belt illustrated by the anisotropy of magnetic susceptibility and fabric modelling. Geological Journal. 2019;**54**:3681-3699.

[18] René M. Source compositions and melting temperatures of the main granitic suites from the Moldanubian batholith. Journal of Geosciences. 2016;**61**:355-370. DOI: 10.3190/

[19] Fuchs G. Exkursion III/4: Kristallin Mühlviertel und Sauwald, südliche Böhmische Masse. Mitteilungen der Geologische Gesellschaft.

Rajpoot GS. Atlas of Plutonic Rocks and

[20] Klomínský J, Jarchovský T,

DOI: 10.1002/gj.3335

jgeosci.223

1964;**57**:281-289

1999;**84**:1781-1792

geosci.004

Tectonophysics. 1995;**248**:97-116. DOI: 10.1016/0040-1951(95)00003-6

Orthogneisses in the Bohemian Massif. 2. Moldanubicum. 1st ed. Prague: Czech

Geological Survey; 2010. p. 200

[22] Friedl G. Geologisch-

Salzburg; 1990

[21] Klob H. Freistädter Granodiorit im österreichischen Moldanubikum. Verhandlungen der Geologische Bundesanstalt. 1971;**1**:98-142

petrographische Untersuchungen in der Gegend nordöstlich von Freistadt (Oberösterreich) mit besonderer Berücksichtigung des "Grabengranits" [thesis]. Salzburg: University of

[23] Klötzli US, Koller F, Scharbert S, Höck V. Cadomian lower-crustal contributions to Variscan Granit Petrogenesis (south bohemian pluton, Austria): Constraints from zircon typology and geochemistry, whole-rock, and feldspar Pb-Sr isotope systematics. Journal of Petrology. 2001;**42**:1621-1642.

DOI: 10.1093/petrology/42.9.1621

[24] Finger F, Gerdes A, Verner K, Žák J. Resolving the growth history of the South Bohemian Batholith by means of high-precision ID-TIMS U-Pb zircon and monazite dating. In: Proceedings of the 3rd Workshop on Orogenic Processes in the Bohemian Massif; 15-17 June 2018; Presseck; 2018. pp. 13-14

[25] Gerdes A, Friedl G, Parrish RR, von Quadt A, Finger F. U-Pb-Datierungen

ICP-MS) an Zirkonen und Monaziten Südböhmischer Granitoide. Erlangen

[26] Gerdes A, Friedl G, Parrish RR, Finger F. High-resolution geochronology of Variscan granite emplacement—The south bohemian batholith. Journal of the Czech Geological Society.

[27] Boyton WV. Geochemistry of the rare earth elements: Meteorite

(TIMS, SHRIMP und LA-MC-

Geologische Abhandlungen. 2002;**Sonderband 4**:30-32

2003;**48**:53-54

**16**

[28] Pouchou JL, Pichoir F. PAP (φ-ρ-Z) procedure for improved quantitative microanalysis. In: Armstrong JT, editor. Microbeam Analysis. San Francisco: San Francisco Press; 1985. pp. 104-106

[29] Richard R. MinPet: mineralogical and petrological data processing system, version 2.02. Québec, Canada: MinPet Geological Software; 1995

[30] Stöbich DM. Trachstudien an den akzessorischen Zirkonen des Weinsberger Granits im östlichen Mühlviertel und westlichen Waldviertel [thesis]. Salzburg: University of Salzburg; 1992

[31] Gerdes A. Magma homogenisation during anataxis, ascent and/or emplacement? Constraints from the Variscan Weinsberg granites. Terra Nova. 2001;**13**:305-312. DOI: 10.1046/j.1365-3121.2001.00365.x

[32] Fuchs G. Zur Altersgliederung des Moldanubikums Oberösterreichs. Vienna: Verhandlungen der Geologische Bundesanstalt; 1962. pp. 96-117

[33] René M, Matějka D, Nosek T. Geochemical constraints on the origin of a distinct type of two-mica granites (Deštná–Lásenice type) in the Moldanubian batholith (Czech Republic). Acta Montana, Geodynamics. Series A. 2003;**23**:59-76

[34] René M, Holtz F, Luo C, Beermann O, Stelling J. Biotite stability in peraluminous granitic melts: Compositional dependence and application to the generation of twomica granites in the South Bohemian batholith (Bohemian Massif, Czech Republic). Lithos. 2008;**102**:538-553. DOI: 10.1016/j.lithos.2007.07.022

[35] Finger F, Clemens J. Migmatization and "secondary" granitic magmas: Effects of emplacement and crystallization of "primary" granitoids in southern Bohemian Massif, Austria. Contributions to Mineralogy and Petrology. 1995;**120**:311-326. DOI: 10.1007/BF00306510

[36] Matějka D, Janoušek V. Wholerock geochemistry and petrogenesis of granites from the northern part of the Moldanubian Batholith (Czech Republic). Acta Universitatis Carolineae, Geology. 1998;**42**:73-79

[37] Sylvester PJ. Post-collisional strongly peraluminous granites. Lithos. 1998;**45**:29-44. DOI: 10.1016/ S0024-4937(98)00024-3

[38] Watson EB, Harrison TM. Zircon saturation revisited: Temperature and composition effects in a variety of crustal magma types. Earth and Planetary Science Letters. 1983;**64**:295-304. DOI: 10.1016/0012-821X(83)90211-X

[39] Boehnke P, Watson EB, Trail D, Harrison TM, Schmitt AK. Zircon saturation re-revisited. Chemical Geology. 2013;**351**:324-334. DOI: 10.1016/j.chemgeo.2013.05.028

[40] Montel JM. A model for monazite/ melt equilibrium and applications to the generation of granitic magmas. Chemical geology. 1993;**110**:127-146

[41] Miller CF. Hot and cold granites? Implications of zircon saturation temperatures and preservation of inheritance. Geology. 2003;**31**:529-532. DOI: 10.1130/0091-7613(2003)031

[42] Siégel C, Bryan SE, Allen CM, Gust DA. Use and abuse of zircon-based thermometers: A critical review and a recommended approach to identify atecrystic zircon. Earth-Science Reviews. 2018;**176**:87-116. DOI: 10.1016/j.earscirev.2017.08.011

[43] Clemens JD, Stevens G, Bryan SE. Conditions during the formation of granitic magmas by crustal melting— Hot or cold; drenched, damp or dry? Earth-Science Reviews. 2020;**200**:1-21. DOI: 10.1016/j.earscirev.2019.102982

[44] René M. Occurrence of Th, U, Y, Zr and REE-bearing accessory minerals on granites and their petrogenetic significance. In: Blasik M, Bogdaska H, editors. Granite, Occurrence, Mineralogy an Origin. 1st ed. New York: Nova Science Publishers, Inc.; 2012. pp. 27-56

[45] Finger F, Gerdes A, Janoušek V, René M, Riegler G. Resolving the Variscan evolution of the Moldanubian sector of the Bohemian Massif: The significance of the Bavarian and the Moravo-Moldanubian tectonometamorphic phases. Journal of Geosciences. 2007;**52**:9-28. DOI: 10.3190/j.geosci.005

**19**

**Chapter 2**

Egypt

**Abstract**

*Gaafar A. El Bahariya*

emplaced between 600 and 475 Ma.

Egypt, older and younger granites, tectonic setting

An Overview on the Classification

Granites constitute the main rock components of the Earth's continental crust, which suggested to be formed in variable geodynamics environments. The different types of granitic rocks, their compositional characteristics, tectonic settings and magma sources are outlined. Mineralogical classification of granites includes four rock types: tonalites, granodiorites, granite (monzogranite and syenogranites) and alkali-feldspar granites. Alphabetical classification subdivided granites into: I-type, S-type, A-type and M-type granites. Moreover, formation of granitic magmas requires distinctive geodynamic settings such as: volcanic arc granite (Cordilleran); collision-related granites (leucogranites); intra-plate and ocean ridge granites. The Eastern Desert of Egypt (ED) forms the northern part of Nubian Shield. Both older and younger granites are widely exposed in the ED. Old granites (OG) comprise tonalites and granodiorites of syn- to late-orogenic granitoid assemblages. They are calcalkaline, I-type, metaluminous and display island arc tectonic setting. Younger granites (YG) on the other hand, include granites, alkali-feldspar granites and minor granodiorites. They are of I- and A-type granites and of post-orogenic to anorogenic tectonic settings. The majority of the YG are alkaline, A-type granite and of within-plate tectonic setting (WPG). The A-type granites are subdivided into: A2-type postorogenic granites and A1-type anorogenic granites. Granite magma genesis involves: (a) fractional crystallization of mafic mantle-derived magmas; (b) anatexis or assimilation of old, upper crustal rocks (c) re - melting of juvenile mafic mantle – derived rocks underplating the continental crust. Generally, older I-type granitoids were interpreted to result from melting of mafic crust and dated at approximately 760–650 Ma, whereas younger granites suggested to be formed as a result of partial melting of a juvenile Neoproterozoic mantle source. Moreover, they formed from anatectic melts of various crustal sources that

**Keywords:** granitoid rocks, neoproterozoic, granites, Nubian shield, Eastern Desert,

Neoproterozoic Granites of the

Nubian Shield, Eastern Desert,

and Tectonic Setting of

#### **Chapter 2**

*Geochemistry*

[43] Clemens JD, Stevens G, Bryan SE. Conditions during the formation of granitic magmas by crustal melting— Hot or cold; drenched, damp or dry? Earth-Science Reviews. 2020;**200**:1-21. DOI: 10.1016/j.earscirev.2019.102982

[44] René M. Occurrence of Th, U, Y, Zr and REE-bearing accessory minerals on granites and their petrogenetic significance. In:

Inc.; 2012. pp. 27-56

10.3190/j.geosci.005

Blasik M, Bogdaska H, editors. Granite, Occurrence, Mineralogy an Origin. 1st ed. New York: Nova Science Publishers,

[45] Finger F, Gerdes A, Janoušek V, René M, Riegler G. Resolving the Variscan evolution of the Moldanubian

sector of the Bohemian Massif: The significance of the Bavarian and the Moravo-Moldanubian tectonometamorphic phases. Journal of Geosciences. 2007;**52**:9-28. DOI:

**18**
