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VOJTĚCH JANOUŠEK, D. R. BOWES, GRAEME ROGERS, COLIN M. FARROW, EMIL JELÍNEK, Modelling Diverse Processes in the Petrogenesis of a Composite Batholith: the Central Bohemian Pluton, Central European Hercynides, Journal of Petrology, Volume 41, Issue 4, April 2000, Pages 511–543, https://doi.org/10.1093/petrology/41.4.511
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Abstract
The multiple intrusions making up the Central Bohemian Pluton in the Central European Hercynides have petrographic and geochemical features consistent with the presence of four main granitoid suites. Major-element, trace-element and Sr–Nd isotopic compositions are used to model their petrogenesis. Partial melting of metabasic rocks or of a CHUR-like mantle source are interpreted to have produced melts parental to the most primitive calc-alkaline Sázava suite. Interaction of basic with more acidic magmas followed by extensive amphibole–plagioclase-dominated fractionation accounts for the production of trondhjemites. Alternatively, the trondhjemites correspond to small-degree melts of a metabasic source. AFC (assimilation–fractional crystallization) modelling with a paragneiss as a contaminant and increasing DNd values simulates the characteristics of the Blatná suite. Closed-system fractionation of strongly enriched mantle-derived magmas or their interaction with leucogranitic melts is deduced for the petrogenesis of the shoshonitic Čertovo břemeno suite. Partial melting of a metasedimentary source, followed by K-feldspar-dominated fractionation, accounts for the granites of the Říčany suite. The progression from relatively primitive calc-alkaline granitoids towards evolved, K-rich calc-alkaline and shoshonitic rocks is interpreted to reflect the increasing enriched mantle input in the petrogenesis of the later suites. The evidence for Hercynian subduction is equivocal and the mantle enrichment could have been significantly older.
INTRODUCTION
The 3200 km2 Central Bohemian Pluton (CBP; Fig. 1) in the Czech Republic is one of the largest composite granitoid complexes in the Central European Hercynides. What makes it special is its great compositional variation, ranging from gabbro, diorite, quartz monzonite, tonalite, trondhjemite and granodiorite to granite (Holub et al., 1997b). Melanocratic K-rich syenites to melagranites also occur, with several of the more mafic types corresponding to rocks of the durbachite suite (Holub, 1989, 1997). As a consequence, the CBP offers an excellent opportunity, within a restricted geographical area, for assessing the nature of the petrogenetic processes that give rise to a composite batholith, particularly in the context of the Central European Hercynides.
The aim of this study is to characterize the whole-rock major- and trace-element geochemistry of some of the larger intrusions covering much of both the overall time-span of the CBP and the range of geochemical variation, complementing published Sr–Nd isotopic data (Janoušek et al., 1995). Geochemical criteria are established for distinguishing cognate groups of intrusions and a petrogenetic model is formulated to account for the observed variations. This model, based upon combined modelling of major elements, trace elements and Sr–Nd isotopes, allows constraints to be placed on the possible sources and processes that were involved in the genesis of the granitoid rocks of the CBP.
REGIONAL SETTING OF THE CBP
The CBP has intruded a major NE–SW trending tectonic zone, the Central Bohemian Suture, which forms the boundary between the Teplá–Barrandian unit (mainly weakly metamorphosed or unmetamorphosed Upper Proterozoic–mid-Devonian sediments) in the NW and the Moldanubian unit (a tectonic assemblage of medium- to high-grade metamorphic rocks of early Proterozoic to early Palaeozoic age) in the SE (Fig. 1) (e.g. Blížkovský et al., 1992). This tectonic zone may represent a ramp region in a major shear zone, which could have exerted a significant control on the emplacement of the CBP (Košler et al., 1995).
Roof pendants within the batholith include a belt of Proterozoic to Lower Palaeozoic (to mid-Devonian: Chaloupský et al., 1995) metasediments and basic volcanic rocks (Metamorphic Islet Zone), tonalitic–granodioritic orthogneisses, which are tectonothermally modified mid–late Devonian calc-alkaline granitoids (Mirotice, Staré Sedlo and Lašovice complexes: Košler, 1993; Košler et al., 1993) and Upper Proterozoic volcanic and volcanogenic rocks (Jílové zone). The contacts of the CBP with both the roof pendants and the Teplá–Barrandian unit are sharp, with a strong thermal metamorphism. In many places the Moldanubian unit adjacent to the CBP has been intensely migmatized.
Mainly on the basis of their distinct appearance in the field, more than 20 major intrusions or ‘rock types’ have been recognized in the CBP. In addition, dozens of other names exist, either for minor intrusions or simply as a continuation of historical tradition. Most of the rocks, however, fall into several distinct groups or suites on the basis of their petrography and geochemical characteristics. An approach that involves only a limited number of suites both helps in genetic interpretations and reduces the plethora of names for the intrusions. Such an approach is analogous to that used in the Lachlan Fold Belt of eastern Australia (e.g. White & Chappell, 1988) with each suite having its own identity in terms of relative age, modal and chemical compositions, textures, enclave and dyke-swarm populations. The classification of the CBP adopted here follows that of Janoušek (1994) and Janoušek et al. (1995) slightly modified from Holub (1992) (Fig. 1; see Holub et al., 1997b), with the following main suites (named after the most prominent intrusion): Sázava, Blatná, Čertovo břemeno and Říčany. Neither rocks of the Maršovice suite, regionally rather insignificant peraluminous S-type granitoids (Holub et al., 1997b), nor small leucogranitic bodies distributed mainly in the eastern CBP, were investigated. On the other hand, data are presented for minette dykes, which cut mainly rocks of the Blatná suite: their petrographic and geochemical characters are consistent with being the most primitive members of the Čertovo břemeno suite.
Geological evidence (Janoušek et al., 1995; Holub et al., 1997b, and references therein) points to a late Devonian–early Carboniferous age for most of the CBP. This is supported by Pb–Pb single-zircon evaporation ages for the Sázava (349 ± 12 Ma), Požáry (351 ± 11 Ma; both Sázava suite), Blatná (346 ± 10 Ma) and Čertovo břemeno (343 ± 6 Ma) intrusions (Holub et al., 1997a) as well as by conventional U–Pb zircon ages for the Klatovy (349+6−4) Ma and Nýrsko (341 ± 2 Ma) intrusions (both Blatná suite; Dörr et al., 1998). 40Ar/39Ar biotite ages of 339 ± 10 Ma (Klatovy intrusion: Dörr et al., 1998), 342 ± 8 Ma (Nýrsko intrusion: Dörr et al., 1998), 336 Ma (Čertovo břemeno intrusion: Matte et al., 1990) and 336 ± 3·5 Ma (Říčany intrusion: H. Maluski, personal communication, 1995) represent cooling ages.
PETROGRAPHY
Sázava suite
Much of the northern CBP is formed by the irregularly shaped Sázava intrusion (Fig. 1) composed of amphibole–biotite to biotite–amphibole quartz diorite, tonalite and granodiorite. It contains about 40–75% plagioclase, 2–35% magnesio-hornblende, 15–35% quartz, ∼10% biotite and 0–12% K-feldspar; common accessory minerals include titanite, apatite, zircon, allanite, epidote and opaque minerals [see Kodymová & Vejnar (1974) for a detailed account of accessory minerals in all major intrusions of the CBP]. Although the typical Sázava plagioclase is unzoned and of andesine composition, some crystals show discontinuous zoning with cores of andesine–labradorite, and rims of sodic andesine. The intrusion contains abundant mafic microgranular enclaves (MME) and much scarcer, mainly metabasic, country-rock xenoliths. This, coupled with the absence of surmicaceous enclaves (Didier & Barbarin, 1991), suggests a negligible metasedimentary but a significant basic igneous input.
At the western margin of the Sázava intrusion there are small bodies of fine-grained quartz diorite with plagioclase megacrysts (Teletín quartz diorite). This unit contains acicular apatites, oikocrysts of quartz and K-feldspar [similar to textures described by Vernon (1991)] and zoned amphiboles with pargasite and magnesio-hastingsite cores, resorbed and overgrown by magnesio-hornblende similar in composition to the amphiboles common in the adjacent Sázava intrusion. Plagioclase is often discontinuously zoned, with resorbed bytownite–anorthite cores overgrown by andesine–labradorite rims, the latter corresponding to the unzoned plagioclase of the matrix. Such mineralogical features are consistent with a hybrid origin of the body (Janoušek et al., 1997a). Other numerous bodies of pyroxene–amphibole gabbro, some with olivine, together with less frequent gabbrodiorite, (quartz) diorite and rare hornblendite are also associated with the Sázava intrusion.
The Požáry intrusion is composed of biotite trondhjemite and leucocratic quartz diorite (55–70% plagioclase, 20–30% quartz, 5% K-feldspar, 4–8% biotite, typically without amphibole). It is poor in apatite and zircon; the main accessory mineral is magnetite. The intrusion frequently contains mantled oligoclase–andesine megacrysts, whose rims have the same composition (sodic andesine) as the unzoned plagioclase of the matrix. Enclaves are generally sparse; the numbers of MME and metasedimentary xenoliths increase towards the contacts with the Sázava intrusion and the Teplá–Barrandian unit, respectively.
Blatná suite
Granodiorites predominate in the central part of the CBP. The elongate, NE-trending Kozárovice intrusion is formed by biotite–amphibole to amphibole–biotite granodiorite (30–45% plagioclase, 10–30% K-feldspar, 10–20% quartz, 10–20% biotite and up to 20% amphibole). K-feldspar phenocrysts vary in abundance, being most numerous in the central part of the body. Apatite, titanite, zircon and opaque minerals are common accessories. The intrusion contains abundant enclaves, including country-rock xenoliths (hornfels, amphibolite, calc-silicates), MME and surmicaceous enclaves. Some of the large bodies of amphibole ± pyroxene ± quartz monzonite–monzogabbro associated with the Blatná suite show evidence for interaction with the surrounding granodiorite (such as quenched apatites, mantled plagioclases and resorbed biotites within mainly euhedral amphiboles) indicating that the magmas that crystallized to form the monzonitic rocks and granodiorites were contemporaneous and interacted with each other (e.g. Kozárovice quartz monzonite: Janoušek, 1994; Janoušek et al., 1997a).
The amphibole–biotite (common mainly at the margins) to biotite (common in the centre of the intrusion) granodiorite of the Blatná intrusion contains 20–35% quartz, 25–45% plagioclase, 5–30% K-feldspar, 15–25% biotite and up to 5% amphibole, with accessory apatite, zircon, titanite, allanite and opaque minerals. The granodiorite is either equigranular or contains a minor proportion of K-feldspar phenocrysts. In the southern part of the intrusion, there is a more mafic facies which has a strong planar fabric (termed the Červená type). The MME and surmicaceous enclaves are generally common but less so in the amphibole-poor granodiorites, which occur mainly in the central part of the intrusion. Country-rock xenoliths (mainly migmatitic and biotite paragneisses, and, more rarely, carbonate rocks and orthogneisses) are also less frequent in the biotite facies, but show a marked increase in number towards roof pendants and the Moldanubian unit.
Plagioclase in the Kozárovice and Blatná intrusions is mainly normally zoned andesine. Less frequently it has labradorite cores or spikes that may point to interaction with basic magma (see Janoušek et al., 1997a).
Čertovo břemeno suite
The NE-trending elongate Sedlčany intrusion comprises porphyritic amphibole–biotite to biotite granite (20–40% quartz, 20–35% plagioclase, 8–40% K-feldspar, 15–25% biotite, and up to 4% amphibole). The most prominent accessory minerals are apatite, zircon, titanite, allanite and opaque minerals. The plagioclase is a relatively homogeneous andesine, with rare oligoclase rims and fracture infillings. Plagioclase crystals enclosed by K-feldspar phenocrysts are usually overgrown by a thin rim of exsolved albite probably of subsolidus origin. Metasedimentary xenoliths, mainly of biotite hornfels, paragneiss, quartz and calc-silicate rock, become more abundant in the western and southwestern parts. MME are also common but surmicaceous enclaves are considerably rarer.
The Čertovo břemeno intrusion is composed of porphyritic amphibole–biotite melagranite and melasyenite resembling the generally coeval K-rich magmatic rocks of the Black Forest, Germany (durbachites; Holub, 1989, 1997). A roughly circular body of biotite–pyroxene syenite to melagranite (with hypersthene and clinopyroxene)—the Tábor syenite—occurs further to the south (Fig. 1).
Říčany suite
The Říčany intrusion in the northernmost part of the CBP (Janoušek et al., 1997c) comprises a porphyritic biotite granite (∼35% K-feldspar, 30% plagioclase, 30% quartz and 5% biotite) with a variable but minor proportion of muscovite (<2%). Apatite and opaque minerals are common accessories; zircon is rarer. The plagioclase is mainly oligoclase; that within K-feldspar phenocrysts has been overgrown by exsolved albite. Various types of enclaves, including MME, surmicaceous enclaves and metasedimentary xenoliths (the latter mainly close to the contact with the Teplá–Barrandian unit) are abundant.
WHOLE-ROCK GEOCHEMISTRY
Major elements
The major-element characteristics of the individual intrusions of the CBP and their grouping into cogenetic suites have recently been reviewed by Holub (1992) and Holub et al. (1997b). Consequently, the major-element data are discussed only briefly here.
In the AFM diagram (Fig. 2), four distinct groups can be distinguished, with each of the Sázava, Blatná and Čertovo břemeno suites forming a progressively shallower calc-alkaline trend and the Říčany suite plotting close to the A apex. In a SiO2–K2O plot (Fig. 3), the relatively low potassium content designates the Sázava suite as being largely calc-alkaline, whereas the Blatná suite is high-K calc-alkaline and both the Čertovo břemeno and Říčany suites, together with the monzonitic rocks of the Blatná suite, are shoshonitic in character.
In terms of alumina saturation (Table 1), some rocks of the Sázava suite are metaluminous (A/CNK < 1; Sázava intrusion and associated mafic rocks), whereas the Požáry trondhjemite falls within the peraluminous domain (A/CNK > 1). In the Blatná suite, the Kozárovice granodiorite and monzonitic rocks are generally metaluminous, whereas the rest of the suite tends to be peraluminous. The more mafic members of the Čertovo břemeno suite are mainly metaluminous (Čertovo břemeno and Tábor intrusions) but the Sedlčany granite straddles the boundary of the peraluminous domain. The Říčany suite is almost exclusively peraluminous.
Sázava suite | Blatná suite | |||||||||||||||||
Intrusion: | Sázava | Teletín | gbd | Požáry | Kozárovice | monzonitic rocks | ||||||||||||
qtzd | ||||||||||||||||||
Sample: | Sa-1 | Sa-4 | Sa-7 | Sa-11 | SaD-1 | Gbs-2 | Po-1 | Po-4 | Koz-2 | Koz-4 | Koz-5 | Koz-6 | Koz-9 | Koz-12 | KozD-1 | Zal-1 | Gbl-1 | Gbl-2 |
Locality: | 1 | 1 | 2 | 3 | 4 | 5 | 6 | 7 | 8 | 9 | 9 | 10 | 11 | 12 | 13 | 14 | 15 | 16 |
SiO2 | 59·98 | 50·72 | 57·73 | 63·72 | 52·90 | 48·84 | 62·95 | 71·09 | 62·92 | 64·79 | 65·53 | 62·59 | 57·69 | 64·60 | 59·58 | 54·22 | 49·21 | 49·62 |
TiO2 | 0·63 | 0·83 | 0·95 | 0·53 | 1·35 | 0·34 | 0·28 | 0·30 | 0·61 | 0·52 | 0·45 | 0·67 | 0·79 | 0·57 | 0·72 | 0·96 | 1·02 | 0·60 |
Al2O3 | 16·42 | 17·57 | 18·82 | 15·63 | 18·23 | 21·64 | 20·02 | 15·09 | 15·69 | 15·28 | 15·43 | 15·66 | 15·81 | 14·99 | 14·80 | 15·24 | 13·69 | 9·06 |
Fe2O3 | 1·35 | 2·19 | 1·00 | 1·31 | 1·47 | 3·28 | 0·67 | 0·38 | 0·86 | 0·96 | 1·46 | 1·08 | 2·11 | 1·27 | 1·69 | 1·17 | 2·47 | 1·64 |
FeO | 5·46 | 7·65 | 5·43 | 4·44 | 7·24 | 2·74 | 1·65 | 2·12 | 3·51 | 2·95 | 2·34 | 3·91 | 4·07 | 2·79 | 4·08 | 6·12 | 6·96 | 6·49 |
MnO | 0·19 | 0·24 | 0·12 | 0·14 | 0·16 | 0·13 | 0·05 | 0·06 | 0·10 | 0·08 | 0·09 | 0·09 | 0·13 | 0·08 | 0·14 | 0·15 | 0·15 | 0·15 |
MgO | 3·21 | 5·18 | 2·82 | 2·13 | 3·89 | 5·11 | 0·55 | 0·52 | 2·96 | 2·33 | 2·14 | 2·72 | 4·70 | 2·37 | 4·11 | 4·94 | 8·53 | 15·07 |
CaO | 7·04 | 9·92 | 7·47 | 5·24 | 8·55 | 13·75 | 6·61 | 3·75 | 4·65 | 4·10 | 3·76 | 4·54 | 5·39 | 3·44 | 5·33 | 7·17 | 9·74 | 8·83 |
Na2O | 2·52 | 2·83 | 2·54 | 3·38 | 2·76 | 1·78 | 3·91 | 3·68 | 3·30 | 3·07 | 3·25 | 2·97 | 3·15 | 3·12 | 2·84 | 2·44 | 1·89 | 1·02 |
K2O | 2·50 | 1·60 | 1·67 | 1·75 | 1·45 | 0·83 | 1·99 | 1·87 | 4·01 | 3·95 | 4·14 | 3·77 | 3·99 | 4·34 | 4·19 | 4·70 | 3·61 | 3·27 |
P2O5 | 0·16 | 0·19 | 0·37 | 0·12 | 0·26 | 0·04 | 0·07 | 0·07 | 0·26 | 0·24 | 0·21 | 0·24 | 0·26 | 0·21 | 0·37 | 0·80 | 0·76 | 0·38 |
H2O+ | 1·18 | 1·17 | 1·14 | 0·87 | 1·53 | 1·57 | 0·71 | 0·71 | 0·88 | 0·80 | 0·72 | 0·97 | 1·02 | 0·97 | 1·34 | 1·48 | 2·05 | 2·55 |
CO2 | 0·18 | 0·09 | 0·13 | 0·34 | 0·06 | 0·51 | 0·35 | 0·27 | 0·13 | 0·03 | 0·06 | 0·05 | 0·26 | 0·21 | 0·19 | 0·05 | 0·16 | 0·11 |
Total | 100·82 | 100·18 | 100·19 | 99·60 | 99·85 | 100·56 | 99·81 | 99·91 | 99·88 | 99·10 | 99·58 | 99·26 | 99·37 | 98·96 | 99·38 | 99·44 | 100·24 | 98·79 |
Mg/(Fe+Mg) | 0·46 | 0·49 | 0·44 | 0·40 | 0·45 | 0·62 | 0·30 | 0·27 | 0·55 | 0·52 | 0·51 | 0·50 | 0·58 | 0·52 | 0·57 | 0·55 | 0·62 | 0·77 |
K/Rb | 273·1 | 237·2 | 243·2 | 227·0 | 279·9 | 222·3 | 323·9 | 267·6 | 232·8 | 204·9 | 197·5 | 230·1 | 188·2 | 208·3 | 186·0 | 176·5 | 194·6 | 158·7 |
A/CNK | 0·84 | 0·72 | 0·96 | 0·92 | 0·84 | 0·75 | 0·97 | 1·01 | 0·86 | 0·91 | 0·93 | 0·91 | 0·82 | 0·93 | 0·78 | 0·69 | 0·55 | 0·43 |
Ba | 1037 | 388 | 722 | 1476 | 1017 | 245 | 1024 | 1284 | 1492 | 1135 | 1286 | 1289 | 1681 | 1154 | 1175 | 2224 | 2329 | 1351 |
Rb | 76 | 56 | 57 | 64 | 43 | 31 | 51 | 58 | 143 | 160 | 174 | 136 | 176 | 173 | 187 | 221 | 154 | 171 |
Sr | 539 | 472 | 537 | 378 | 430 | 278 | 599 | 430 | 500 | 430 | 418 | 409 | 519 | 385 | 379 | 510 | 540 | 218 |
Zr | 76 | 56 | 57 | 74 | 88 | 27 | 128 | 180 | 216 | 201 | 201 | 218 | 251 | 211 | 146 | 251 | 62 | 77 |
Nb | 6 | 5 | 10 | 5 | 10 | 8 | 5 | 6 | — | — | 14 | 13 | 16 | 11 | 9 | 16 | 11 | 7 |
Ga | 17 | 19 | 20 | 16 | 18 | 14 | 18 | 14 | 18 | 18 | 17 | 20 | 17 | 16 | 20 | 19 | 18 | 14 |
Cr | 29 | 53 | 33 | 50 | 43 | 159 | 15 | 16 | 84 | 99 | 113 | 76 | 147 | 57 | 171 | 198 | 496 | 1283 |
Ni | 10 | b.d. | b.d. | b.d. | b.d. | 13 | b.d. | b.d. | 18 | 20 | 19 | 18 | 28 | 17 | 66 | 17 | 71 | 233 |
Co | 17 | 30 | 13 | 13 | 18 | 23 | b.d. | 4 | 9 | 10 | 13 | 12 | 13 | 12 | 20 | 25 | 37 | 57 |
Pb | 22 | 15 | 13 | 15 | b.d. | 13 | 21 | 29 | 34 | 37 | 46 | 29 | 31 | 36 | 42 | 31 | 19 | 12 |
Zn | 71 | 104 | 50 | 73 | 85 | 51 | 23 | 22 | 52 | 50 | 49 | 60 | 69 | 52 | 85 | 85 | 85 | 59 |
La | — | 21·7 | 20·8 | — | 20·0 | — | 11·6 | 26·2 | 35·0 | — | — | 34·8 | — | 32·7 | 25·9 | 43·9 | 27·7 | 26·0 |
Ce | — | 71·8 | 42·0 | — | 46·8 | — | 18·0 | 39·0 | 64·4 | — | — | 68·3 | — | 58·4 | 58·3 | 94·3 | 60·3 | 54·1 |
Pr | — | 6·9 | 5·0 | — | 6·1 | — | 1·8 | 3·9 | 7·9 | — | — | 8·2 | — | 7·3 | 7·8 | 11·7 | 7·7 | 7·1 |
Nd | — | 29·7 | 17·4 | — | 23·5 | — | 5·4 | 11·5 | 27·5 | — | — | 29·4 | — | 24·9 | 28·6 | 45·5 | 29·2 | 26·0 |
Sm | — | 6·2 | 3·8 | — | 5·9 | — | 1·4 | 1·8 | 5·7 | — | — | 6·0 | — | 4·9 | 5·9 | 10·0 | 7·0 | 6·4 |
Eu | — | 1·5 | 1·8 | — | 2·0 | — | 1·3 | 1·0 | 1·5 | — | — | 1·6 | — | 1·3 | 1·5 | 2·5 | 2·2 | 1·6 |
Gd | — | 6·1 | 3·8 | — | 6·2 | — | 1·1 | 1·4 | 4·7 | — | — | 5·3 | — | 4·3 | 4·9 | 8·4 | 7·0 | 5·8 |
Tb | — | 0·9 | 0·6 | — | 1·0 | — | 0·1 | 0·2 | 0·7 | — | — | 0·8 | — | 0·6 | 0·7 | 1·0 | 0·7 | 0·8 |
Dy | — | 5·8 | 2·7 | — | 5·1 | — | 0·6 | 0·8 | 3·5 | — | — | 4·1 | — | 3·1 | 3·4 | 5·6 | 3·7 | 4·2 |
Ho | — | 1·0 | 0·6 | — | 1·1 | — | 0·1 | 0·1 | 0·6 | — | — | 0·7 | — | 0·6 | 0·6 | 1·0 | 0·7 | 0·8 |
Er | — | 2·8 | 1·6 | — | 2·8 | — | 0·4 | 0·5 | 1·8 | — | — | 2·1 | — | 1·7 | 1·8 | 2·8 | 1·8 | 2·2 |
Tm | — | 0·4 | 0·2 | — | 0·5 | — | 0·1 | 0·1 | 0·3 | — | — | 0·3 | — | 0·2 | 0·3 | 0·4 | 0·2 | 0·3 |
Yb | — | 2·9 | 1·5 | — | 2·7 | — | 0·5 | 0·6 | 1·7 | — | — | 2·0 | — | 1·6 | 1·8 | 2·5 | 1·6 | 2·0 |
Lu | — | 0·4 | 0·2 | — | 0·5 | — | 0·1 | 0·1 | 0·3 | — | — | 0·3 | — | 0·3 | 0·3 | 0·4 | 0·2 | 0·3 |
∑REE | — | 158·2 | 101·9 | — | 124·3 | — | 42·4 | 87·1 | 155·6 | — | — | 164·0 | — | 141·8 | 141·8 | 230·0 | 150·3 | 137·5 |
Eu/Eu* | — | 0·7 | 1·4 | — | 1·0 | — | 3·2 | 2·1 | 0·9 | — | — | 0·8 | — | 0·8 | 0·8 | 0·8 | 1·0 | 0·8 |
CeN/YbN | — | 6·4 | 7·2 | — | 4·5 | — | 9·2 | 16·6 | 9·6 | — | — | 8·9 | — | 9·4 | 8·2 | 9·6 | 9·9 | 7·1 |
Cs | — | 5·7 | 6·6 | — | 2·3 | — | 3·0 | 3·0 | 9·9 | — | — | 6·8 | — | 13·0 | 21·3 | 17·7 | 7·8 | 13·1 |
Ta | — | 0·5 | 0·6 | — | 1·1 | — | 0·3 | 0·2 | 1·2 | — | — | 0·7 | — | 1·1 | 1·5 | 1·1 | 0·7 | 0·8 |
Hf | — | 2·5 | 3·6 | — | 1·8 | — | 4·2 | 5·4 | 5·8 | — | — | 6·1 | — | 7·2 | 4·7 | 13·3 | 4·3 | 5·0 |
Sázava suite | Blatná suite | |||||||||||||||||
Intrusion: | Sázava | Teletín | gbd | Požáry | Kozárovice | monzonitic rocks | ||||||||||||
qtzd | ||||||||||||||||||
Sample: | Sa-1 | Sa-4 | Sa-7 | Sa-11 | SaD-1 | Gbs-2 | Po-1 | Po-4 | Koz-2 | Koz-4 | Koz-5 | Koz-6 | Koz-9 | Koz-12 | KozD-1 | Zal-1 | Gbl-1 | Gbl-2 |
Locality: | 1 | 1 | 2 | 3 | 4 | 5 | 6 | 7 | 8 | 9 | 9 | 10 | 11 | 12 | 13 | 14 | 15 | 16 |
SiO2 | 59·98 | 50·72 | 57·73 | 63·72 | 52·90 | 48·84 | 62·95 | 71·09 | 62·92 | 64·79 | 65·53 | 62·59 | 57·69 | 64·60 | 59·58 | 54·22 | 49·21 | 49·62 |
TiO2 | 0·63 | 0·83 | 0·95 | 0·53 | 1·35 | 0·34 | 0·28 | 0·30 | 0·61 | 0·52 | 0·45 | 0·67 | 0·79 | 0·57 | 0·72 | 0·96 | 1·02 | 0·60 |
Al2O3 | 16·42 | 17·57 | 18·82 | 15·63 | 18·23 | 21·64 | 20·02 | 15·09 | 15·69 | 15·28 | 15·43 | 15·66 | 15·81 | 14·99 | 14·80 | 15·24 | 13·69 | 9·06 |
Fe2O3 | 1·35 | 2·19 | 1·00 | 1·31 | 1·47 | 3·28 | 0·67 | 0·38 | 0·86 | 0·96 | 1·46 | 1·08 | 2·11 | 1·27 | 1·69 | 1·17 | 2·47 | 1·64 |
FeO | 5·46 | 7·65 | 5·43 | 4·44 | 7·24 | 2·74 | 1·65 | 2·12 | 3·51 | 2·95 | 2·34 | 3·91 | 4·07 | 2·79 | 4·08 | 6·12 | 6·96 | 6·49 |
MnO | 0·19 | 0·24 | 0·12 | 0·14 | 0·16 | 0·13 | 0·05 | 0·06 | 0·10 | 0·08 | 0·09 | 0·09 | 0·13 | 0·08 | 0·14 | 0·15 | 0·15 | 0·15 |
MgO | 3·21 | 5·18 | 2·82 | 2·13 | 3·89 | 5·11 | 0·55 | 0·52 | 2·96 | 2·33 | 2·14 | 2·72 | 4·70 | 2·37 | 4·11 | 4·94 | 8·53 | 15·07 |
CaO | 7·04 | 9·92 | 7·47 | 5·24 | 8·55 | 13·75 | 6·61 | 3·75 | 4·65 | 4·10 | 3·76 | 4·54 | 5·39 | 3·44 | 5·33 | 7·17 | 9·74 | 8·83 |
Na2O | 2·52 | 2·83 | 2·54 | 3·38 | 2·76 | 1·78 | 3·91 | 3·68 | 3·30 | 3·07 | 3·25 | 2·97 | 3·15 | 3·12 | 2·84 | 2·44 | 1·89 | 1·02 |
K2O | 2·50 | 1·60 | 1·67 | 1·75 | 1·45 | 0·83 | 1·99 | 1·87 | 4·01 | 3·95 | 4·14 | 3·77 | 3·99 | 4·34 | 4·19 | 4·70 | 3·61 | 3·27 |
P2O5 | 0·16 | 0·19 | 0·37 | 0·12 | 0·26 | 0·04 | 0·07 | 0·07 | 0·26 | 0·24 | 0·21 | 0·24 | 0·26 | 0·21 | 0·37 | 0·80 | 0·76 | 0·38 |
H2O+ | 1·18 | 1·17 | 1·14 | 0·87 | 1·53 | 1·57 | 0·71 | 0·71 | 0·88 | 0·80 | 0·72 | 0·97 | 1·02 | 0·97 | 1·34 | 1·48 | 2·05 | 2·55 |
CO2 | 0·18 | 0·09 | 0·13 | 0·34 | 0·06 | 0·51 | 0·35 | 0·27 | 0·13 | 0·03 | 0·06 | 0·05 | 0·26 | 0·21 | 0·19 | 0·05 | 0·16 | 0·11 |
Total | 100·82 | 100·18 | 100·19 | 99·60 | 99·85 | 100·56 | 99·81 | 99·91 | 99·88 | 99·10 | 99·58 | 99·26 | 99·37 | 98·96 | 99·38 | 99·44 | 100·24 | 98·79 |
Mg/(Fe+Mg) | 0·46 | 0·49 | 0·44 | 0·40 | 0·45 | 0·62 | 0·30 | 0·27 | 0·55 | 0·52 | 0·51 | 0·50 | 0·58 | 0·52 | 0·57 | 0·55 | 0·62 | 0·77 |
K/Rb | 273·1 | 237·2 | 243·2 | 227·0 | 279·9 | 222·3 | 323·9 | 267·6 | 232·8 | 204·9 | 197·5 | 230·1 | 188·2 | 208·3 | 186·0 | 176·5 | 194·6 | 158·7 |
A/CNK | 0·84 | 0·72 | 0·96 | 0·92 | 0·84 | 0·75 | 0·97 | 1·01 | 0·86 | 0·91 | 0·93 | 0·91 | 0·82 | 0·93 | 0·78 | 0·69 | 0·55 | 0·43 |
Ba | 1037 | 388 | 722 | 1476 | 1017 | 245 | 1024 | 1284 | 1492 | 1135 | 1286 | 1289 | 1681 | 1154 | 1175 | 2224 | 2329 | 1351 |
Rb | 76 | 56 | 57 | 64 | 43 | 31 | 51 | 58 | 143 | 160 | 174 | 136 | 176 | 173 | 187 | 221 | 154 | 171 |
Sr | 539 | 472 | 537 | 378 | 430 | 278 | 599 | 430 | 500 | 430 | 418 | 409 | 519 | 385 | 379 | 510 | 540 | 218 |
Zr | 76 | 56 | 57 | 74 | 88 | 27 | 128 | 180 | 216 | 201 | 201 | 218 | 251 | 211 | 146 | 251 | 62 | 77 |
Nb | 6 | 5 | 10 | 5 | 10 | 8 | 5 | 6 | — | — | 14 | 13 | 16 | 11 | 9 | 16 | 11 | 7 |
Ga | 17 | 19 | 20 | 16 | 18 | 14 | 18 | 14 | 18 | 18 | 17 | 20 | 17 | 16 | 20 | 19 | 18 | 14 |
Cr | 29 | 53 | 33 | 50 | 43 | 159 | 15 | 16 | 84 | 99 | 113 | 76 | 147 | 57 | 171 | 198 | 496 | 1283 |
Ni | 10 | b.d. | b.d. | b.d. | b.d. | 13 | b.d. | b.d. | 18 | 20 | 19 | 18 | 28 | 17 | 66 | 17 | 71 | 233 |
Co | 17 | 30 | 13 | 13 | 18 | 23 | b.d. | 4 | 9 | 10 | 13 | 12 | 13 | 12 | 20 | 25 | 37 | 57 |
Pb | 22 | 15 | 13 | 15 | b.d. | 13 | 21 | 29 | 34 | 37 | 46 | 29 | 31 | 36 | 42 | 31 | 19 | 12 |
Zn | 71 | 104 | 50 | 73 | 85 | 51 | 23 | 22 | 52 | 50 | 49 | 60 | 69 | 52 | 85 | 85 | 85 | 59 |
La | — | 21·7 | 20·8 | — | 20·0 | — | 11·6 | 26·2 | 35·0 | — | — | 34·8 | — | 32·7 | 25·9 | 43·9 | 27·7 | 26·0 |
Ce | — | 71·8 | 42·0 | — | 46·8 | — | 18·0 | 39·0 | 64·4 | — | — | 68·3 | — | 58·4 | 58·3 | 94·3 | 60·3 | 54·1 |
Pr | — | 6·9 | 5·0 | — | 6·1 | — | 1·8 | 3·9 | 7·9 | — | — | 8·2 | — | 7·3 | 7·8 | 11·7 | 7·7 | 7·1 |
Nd | — | 29·7 | 17·4 | — | 23·5 | — | 5·4 | 11·5 | 27·5 | — | — | 29·4 | — | 24·9 | 28·6 | 45·5 | 29·2 | 26·0 |
Sm | — | 6·2 | 3·8 | — | 5·9 | — | 1·4 | 1·8 | 5·7 | — | — | 6·0 | — | 4·9 | 5·9 | 10·0 | 7·0 | 6·4 |
Eu | — | 1·5 | 1·8 | — | 2·0 | — | 1·3 | 1·0 | 1·5 | — | — | 1·6 | — | 1·3 | 1·5 | 2·5 | 2·2 | 1·6 |
Gd | — | 6·1 | 3·8 | — | 6·2 | — | 1·1 | 1·4 | 4·7 | — | — | 5·3 | — | 4·3 | 4·9 | 8·4 | 7·0 | 5·8 |
Tb | — | 0·9 | 0·6 | — | 1·0 | — | 0·1 | 0·2 | 0·7 | — | — | 0·8 | — | 0·6 | 0·7 | 1·0 | 0·7 | 0·8 |
Dy | — | 5·8 | 2·7 | — | 5·1 | — | 0·6 | 0·8 | 3·5 | — | — | 4·1 | — | 3·1 | 3·4 | 5·6 | 3·7 | 4·2 |
Ho | — | 1·0 | 0·6 | — | 1·1 | — | 0·1 | 0·1 | 0·6 | — | — | 0·7 | — | 0·6 | 0·6 | 1·0 | 0·7 | 0·8 |
Er | — | 2·8 | 1·6 | — | 2·8 | — | 0·4 | 0·5 | 1·8 | — | — | 2·1 | — | 1·7 | 1·8 | 2·8 | 1·8 | 2·2 |
Tm | — | 0·4 | 0·2 | — | 0·5 | — | 0·1 | 0·1 | 0·3 | — | — | 0·3 | — | 0·2 | 0·3 | 0·4 | 0·2 | 0·3 |
Yb | — | 2·9 | 1·5 | — | 2·7 | — | 0·5 | 0·6 | 1·7 | — | — | 2·0 | — | 1·6 | 1·8 | 2·5 | 1·6 | 2·0 |
Lu | — | 0·4 | 0·2 | — | 0·5 | — | 0·1 | 0·1 | 0·3 | — | — | 0·3 | — | 0·3 | 0·3 | 0·4 | 0·2 | 0·3 |
∑REE | — | 158·2 | 101·9 | — | 124·3 | — | 42·4 | 87·1 | 155·6 | — | — | 164·0 | — | 141·8 | 141·8 | 230·0 | 150·3 | 137·5 |
Eu/Eu* | — | 0·7 | 1·4 | — | 1·0 | — | 3·2 | 2·1 | 0·9 | — | — | 0·8 | — | 0·8 | 0·8 | 0·8 | 1·0 | 0·8 |
CeN/YbN | — | 6·4 | 7·2 | — | 4·5 | — | 9·2 | 16·6 | 9·6 | — | — | 8·9 | — | 9·4 | 8·2 | 9·6 | 9·9 | 7·1 |
Cs | — | 5·7 | 6·6 | — | 2·3 | — | 3·0 | 3·0 | 9·9 | — | — | 6·8 | — | 13·0 | 21·3 | 17·7 | 7·8 | 13·1 |
Ta | — | 0·5 | 0·6 | — | 1·1 | — | 0·3 | 0·2 | 1·2 | — | — | 0·7 | — | 1·1 | 1·5 | 1·1 | 0·7 | 0·8 |
Hf | — | 2·5 | 3·6 | — | 1·8 | — | 4·2 | 5·4 | 5·8 | — | — | 6·1 | — | 7·2 | 4·7 | 13·3 | 4·3 | 5·0 |
Blatná suite | Čertovo břemeno suite | Říčany s. | ||||||||||||||||
Intrusion: | Blatná | Sedlčany | Čert. bř. | Tábor | minettes | Říčany | ||||||||||||
Sample: | Bl-1 | Bl-2 | Bl-4 | Bl-7 | Bl-8 | Cv-1 | Cv-3 | Se-1 | Se-5 | Se-6 | Se-9 | Se-12 | Se-15 | Cb-3 | Ta-1 | Mi-1 | Mi-2 | Ri-1 |
Locality: | 17 | 18 | 19 | 20 | 21 | 22 | 23 | 24 | 25 | 25 | 24 | 26 | 27 | 28 | 29 | 30 | 31 | 32 |
SiO2 | 67·08 | 63·16 | 68·11 | 67·80 | 62·94 | 62·88 | 61·86 | 66·58 | 65·87 | 66·70 | 67·74 | 69·06 | 66·47 | 55·96 | 59·69 | 58·32 | 56·22 | 71·43 |
TiO2 | 0·50 | 0·79 | 0·52 | 0·49 | 0·70 | 0·76 | 0·73 | 0·60 | 0·63 | 0·56 | 0·54 | 0·53 | 0·60 | 1·07 | 0·91 | 0·88 | 1·45 | 0·30 |
Al2O3 | 14·88 | 16·33 | 15·43 | 15·43 | 15·74 | 16·15 | 16·17 | 14·58 | 14·41 | 14·72 | 14·55 | 14·37 | 14·47 | 13·62 | 14·13 | 12·27 | 12·47 | 14·58 |
Fe2O3 | 0·81 | 0·50 | 0·68 | 0·55 | 0·60 | 0·88 | 0·81 | 0·51 | 0·56 | 0·54 | 0·57 | 0·29 | 0·52 | 2·29 | 0·38 | 1·69 | 1·51 | 0·26 |
FeO | 2·43 | 3·82 | 2·19 | 2·24 | 3·92 | 3·90 | 4·18 | 2·55 | 2·53 | 2·33 | 2·53 | 2·43 | 2·66 | 3·56 | 4·51 | 4·11 | 3·97 | 0·99 |
MnO | 0·06 | 0·07 | 0·05 | 0·05 | 0·11 | 0·07 | 0·10 | 0·06 | 0·06 | 0·07 | 0·07 | 0·03 | 0·06 | 0·13 | 0·08 | 0·10 | 0·09 | 0·01 |
MgO | 1·82 | 2·64 | 1·61 | 1·59 | 3·17 | 3·49 | 3·58 | 2·53 | 2·53 | 2·56 | 2·38 | 2·19 | 2·55 | 7·33 | 5·07 | 8·25 | 7·97 | 1·12 |
CaO | 2·76 | 3·62 | 2·82 | 2·70 | 4·31 | 4·44 | 3·98 | 2·36 | 2·37 | 2·35 | 2·24 | 2·06 | 2·39 | 4·11 | 3·72 | 3·60 | 3·83 | 1·27 |
Na2O | 3·64 | 3·36 | 3·45 | 3·40 | 3·08 | 2·62 | 2·94 | 2·69 | 2·63 | 2·70 | 2·32 | 2·53 | 2·68 | 2·16 | 2·07 | 1·83 | 1·34 | 3·32 |
K2O | 4·07 | 3·57 | 4·12 | 4·38 | 3·55 | 3·67 | 3·56 | 5·80 | 5·85 | 5·69 | 5·54 | 5·36 | 5·62 | 6·67 | 6·82 | 6·12 | 7·20 | 5·29 |
P2O5 | 0·17 | 0·29 | 0·17 | 0·17 | 0·24 | 0·28 | 0·26 | 0·36 | 0·38 | 0·33 | 0·33 | 0·29 | 0·36 | 0·89 | 0·67 | 0·66 | 0·89 | 0·17 |
H2O+ | 1·00 | 0·97 | 0·79 | 0·63 | 1·13 | 1·01 | 1·01 | 0·90 | 0·92 | 0·76 | 0·77 | 0·68 | 0·88 | 1·53 | 0·80 | 1·50 | 2·09 | 0·51 |
CO2 | 0·37 | 0·06 | 0·06 | 0·04 | 0·27 | 0·14 | 0·19 | 0·04 | 0·03 | 0·25 | 0·26 | 0·33 | 0·04 | 0·19 | 0·04 | 0·51 | 0·25 | 0·03 |
Total | 99·59 | 99·18 | 100·00 | 99·47 | 99·76 | 100·29 | 99·37 | 99·56 | 98·77 | 99·56 | 99·84 | 100·15 | 99·30 | 99·51 | 98·89 | 99·84 | 99·28 | 99·28 |
Mg/(Fe+Mg) | 0·51 | 0·52 | 0·51 | 0·51 | 0·56 | 0·57 | 0·57 | 0·60 | 0·60 | 0·62 | 0·58 | 0·59 | 0·59 | 0·70 | 0·65 | 0·72 | 0·73 | 0·62 |
K/Rb | 169·8 | 160·2 | 180·0 | 207·8 | 200·5 | 230·8 | 173·8 | 166·0 | 156·1 | 155·4 | 147·9 | 151·9 | 131·8 | 153·8 | 159·5 | 124·2 | 170·8 | 137·2 |
A/CNK | 0·97 | 1·02 | 1·01 | 1·01 | 0·94 | 0·99 | 1·02 | 0·97 | 0·96 | 0·99 | 1·05 | 1·05 | 0·98 | 0·75 | 0·81 | 0·76 | 0·74 | 1·08 |
Ba | 963 | 1204 | 900 | 928 | 1080 | 1149 | 1181 | 1079 | 1126 | 1115 | 1076 | 1002 | 1084 | 2109 | 1797 | 1578 | 2084 | 901 |
Rb | 199 | 185 | 190 | 175 | 147 | 132 | 170 | 290 | 311 | 304 | 311 | 293 | 354 | 360 | 355 | 409 | 350 | 320 |
Sr | 333 | 413 | 348 | 338 | 361 | 412 | 368 | 318 | 354 | 358 | 312 | 312 | 302 | 495 | 418 | 355 | 350 | 378 |
Zr | 177 | 188 | 171 | 149 | 169 | 226 | 146 | 237 | 283 | 269 | 256 | 259 | 229 | 405 | 390 | 372 | 544 | 240 |
Nb | 12 | 12 | 13 | 18 | 14 | 9 | 14 | 14 | 16 | 17 | 20 | 16 | 19 | 23 | 13 | 20 | — | 21 |
Ga | 21 | 23 | 19 | 20 | b.d. | 23 | 22 | 20 | 20 | 20 | 19 | 18 | 19 | 20 | 19 | 18 | 18 | 24 |
Cr | 61 | 111 | 50 | 54 | 114 | 75 | 131 | 168 | 160 | 132 | 166 | 122 | 157 | 498 | 425 | 504 | 486 | 43 |
Ni | 18 | 25 | 15 | 16 | 31 | 24 | 38 | 33 | 24 | 26 | 30 | 27 | 45 | 135 | 59 | 235 | 127 | 11 |
Co | 8 | 11 | 10 | 7 | 12 | 15 | 16 | 10 | 12 | 12 | 8 | 5 | 12 | 28 | 22 | 28 | 30 | b.d. |
Pb | 40 | 24 | 41 | 43 | 24 | 17 | 34 | 53 | 70 | 68 | 68 | 63 | 60 | 34 | 46 | 53 | 69 | 66 |
Zn | 63 | 79 | 58 | 54 | 51 | 74 | 84 | 55 | 58 | 50 | 53 | 52 | 62 | 85 | 76 | 79 | 70 | 34 |
La | — | 55·2 | 39·8 | 33·1 | 42·9 | 45·6 | — | 109·3 | 43·9 | — | 44·2 | — | 44·5 | 44·8 | 54·0 | 52·6 | — | 18·2 |
Ce | — | 111·1 | 80·9 | 66·2 | 94·6 | 99·6 | — | — | 91·8 | — | 92·3 | — | 96·8 | 110·2 | 125·3 | 119·1 | — | 35·4 |
Pr | — | 12·7 | 9·6 | 8·0 | 11·9 | 12·4 | — | 20·6 | 11·5 | — | 11·7 | — | 11·5 | 15·5 | 17·0 | 15·8 | — | 4·2 |
Nd | — | 42·5 | 31·6 | 26·7 | 43·3 | 44·9 | — | 63·0 | 40·8 | — | 42·1 | — | 39·9 | 61·7 | 62·8 | 58·8 | — | 15·2 |
Sm | — | 7·2 | 5·6 | 5·5 | 9·4 | 9·8 | — | 10·4 | 8·4 | — | 8·8 | — | 8·3 | 14·6 | 13·7 | 13·8 | — | 2·9 |
Eu | — | 1·7 | 1·2 | 1·2 | 1·9 | 1·7 | — | 2·1 | 1·7 | — | 1·8 | — | 1·7 | 3·5 | 2·9 | 3·4 | — | 0·7 |
Gd | — | 5·9 | 4·7 | 4·7 | 8·2 | 9·2 | — | 12·4 | 6·2 | — | 6·4 | — | 6·6 | 10·7 | 10·7 | 10·0 | — | 2·1 |
Tb | — | 0·7 | 0·6 | 0·7 | 1·2 | 1·2 | — | 1·1 | 0·8 | — | 0·9 | — | 0·8 | 1·2 | 1·2 | 1·1 | — | 0·3 |
Dy | — | 3·4 | 3·1 | 3·4 | 5·8 | 6·6 | — | 4·5 | 3·9 | — | 4·1 | — | 4·0 | 5·8 | 5·9 | 5·1 | — | 1·3 |
Ho | — | 0·5 | 0·5 | 0·6 | 1·1 | 1·2 | — | 0·7 | 0·7 | — | 0·7 | — | 0·6 | 0·9 | 1·0 | 0·8 | — | 0·2 |
Er | — | 1·4 | 1·6 | 1·8 | 2·9 | 3·2 | — | 2·0 | 1·9 | — | 2·0 | — | 1·7 | 2·5 | 2·6 | 2·3 | — | 0·6 |
Tm | — | 0·2 | 0·3 | 0·3 | 0·5 | 0·4 | — | 0·3 | 0·3 | — | 0·3 | — | 0·2 | 0·3 | 0·3 | 0·3 | — | 0·1 |
Yb | — | 1·2 | 1·8 | 1·8 | 2·7 | 2·6 | — | 1·9 | 1·7 | — | 1·9 | — | 1·6 | 2·1 | 2·1 | 1·9 | — | 0·6 |
Lu | — | 0·2 | 0·3 | 0·3 | 0·4 | 0·3 | — | 0·3 | 0·3 | — | 0·3 | — | 0·2 | 0·3 | 0·3 | 0·3 | — | 0·1 |
∑REE | — | 244·0 | 181·7 | 154·0 | 226·7 | 238·5 | — | — | 213·9 | — | 217·4 | — | 218·6 | 274·2 | 299·9 | 285·3 | — | 81·9 |
Eu/Eu* | — | 0·8 | 0·7 | 0·7 | 0·7 | 0·5 | — | 0·6 | 0·7 | — | 0·7 | — | 0·7 | 0·8 | 0·7 | 0·9 | — | 0·9 |
CeN/YbN | — | 23·2 | 11·5 | 9·8 | 9·2 | 10·1 | — | — | 13·7 | — | 12·7 | — | 15·7 | 13·6 | 15·5 | 16·0 | — | 15·0 |
Cs | — | 12·2 | 18·8 | 17·4 | 8·5 | 6·4 | — | 30·0 | 51·6 | — | 31·7 | — | 48·9 | 27·0 | 23·7 | 55·5 | — | 66·0 |
Ta | — | 1·4 | 1·4 | 1·7 | 1·5 | 1·0 | — | 2·4 | 2·9 | — | 2·4 | — | 4·4 | 1·8 | 1·7 | 2·2 | — | 2·3 |
Hf | — | 3·8 | 6·3 | 9·9 | 4·5 | 3·3 | — | 6·7 | 8·5 | — | 9·1 | — | 6·7 | 12·8 | 4·3 | 10·8 | — | 8·8 |
Blatná suite | Čertovo břemeno suite | Říčany s. | ||||||||||||||||
Intrusion: | Blatná | Sedlčany | Čert. bř. | Tábor | minettes | Říčany | ||||||||||||
Sample: | Bl-1 | Bl-2 | Bl-4 | Bl-7 | Bl-8 | Cv-1 | Cv-3 | Se-1 | Se-5 | Se-6 | Se-9 | Se-12 | Se-15 | Cb-3 | Ta-1 | Mi-1 | Mi-2 | Ri-1 |
Locality: | 17 | 18 | 19 | 20 | 21 | 22 | 23 | 24 | 25 | 25 | 24 | 26 | 27 | 28 | 29 | 30 | 31 | 32 |
SiO2 | 67·08 | 63·16 | 68·11 | 67·80 | 62·94 | 62·88 | 61·86 | 66·58 | 65·87 | 66·70 | 67·74 | 69·06 | 66·47 | 55·96 | 59·69 | 58·32 | 56·22 | 71·43 |
TiO2 | 0·50 | 0·79 | 0·52 | 0·49 | 0·70 | 0·76 | 0·73 | 0·60 | 0·63 | 0·56 | 0·54 | 0·53 | 0·60 | 1·07 | 0·91 | 0·88 | 1·45 | 0·30 |
Al2O3 | 14·88 | 16·33 | 15·43 | 15·43 | 15·74 | 16·15 | 16·17 | 14·58 | 14·41 | 14·72 | 14·55 | 14·37 | 14·47 | 13·62 | 14·13 | 12·27 | 12·47 | 14·58 |
Fe2O3 | 0·81 | 0·50 | 0·68 | 0·55 | 0·60 | 0·88 | 0·81 | 0·51 | 0·56 | 0·54 | 0·57 | 0·29 | 0·52 | 2·29 | 0·38 | 1·69 | 1·51 | 0·26 |
FeO | 2·43 | 3·82 | 2·19 | 2·24 | 3·92 | 3·90 | 4·18 | 2·55 | 2·53 | 2·33 | 2·53 | 2·43 | 2·66 | 3·56 | 4·51 | 4·11 | 3·97 | 0·99 |
MnO | 0·06 | 0·07 | 0·05 | 0·05 | 0·11 | 0·07 | 0·10 | 0·06 | 0·06 | 0·07 | 0·07 | 0·03 | 0·06 | 0·13 | 0·08 | 0·10 | 0·09 | 0·01 |
MgO | 1·82 | 2·64 | 1·61 | 1·59 | 3·17 | 3·49 | 3·58 | 2·53 | 2·53 | 2·56 | 2·38 | 2·19 | 2·55 | 7·33 | 5·07 | 8·25 | 7·97 | 1·12 |
CaO | 2·76 | 3·62 | 2·82 | 2·70 | 4·31 | 4·44 | 3·98 | 2·36 | 2·37 | 2·35 | 2·24 | 2·06 | 2·39 | 4·11 | 3·72 | 3·60 | 3·83 | 1·27 |
Na2O | 3·64 | 3·36 | 3·45 | 3·40 | 3·08 | 2·62 | 2·94 | 2·69 | 2·63 | 2·70 | 2·32 | 2·53 | 2·68 | 2·16 | 2·07 | 1·83 | 1·34 | 3·32 |
K2O | 4·07 | 3·57 | 4·12 | 4·38 | 3·55 | 3·67 | 3·56 | 5·80 | 5·85 | 5·69 | 5·54 | 5·36 | 5·62 | 6·67 | 6·82 | 6·12 | 7·20 | 5·29 |
P2O5 | 0·17 | 0·29 | 0·17 | 0·17 | 0·24 | 0·28 | 0·26 | 0·36 | 0·38 | 0·33 | 0·33 | 0·29 | 0·36 | 0·89 | 0·67 | 0·66 | 0·89 | 0·17 |
H2O+ | 1·00 | 0·97 | 0·79 | 0·63 | 1·13 | 1·01 | 1·01 | 0·90 | 0·92 | 0·76 | 0·77 | 0·68 | 0·88 | 1·53 | 0·80 | 1·50 | 2·09 | 0·51 |
CO2 | 0·37 | 0·06 | 0·06 | 0·04 | 0·27 | 0·14 | 0·19 | 0·04 | 0·03 | 0·25 | 0·26 | 0·33 | 0·04 | 0·19 | 0·04 | 0·51 | 0·25 | 0·03 |
Total | 99·59 | 99·18 | 100·00 | 99·47 | 99·76 | 100·29 | 99·37 | 99·56 | 98·77 | 99·56 | 99·84 | 100·15 | 99·30 | 99·51 | 98·89 | 99·84 | 99·28 | 99·28 |
Mg/(Fe+Mg) | 0·51 | 0·52 | 0·51 | 0·51 | 0·56 | 0·57 | 0·57 | 0·60 | 0·60 | 0·62 | 0·58 | 0·59 | 0·59 | 0·70 | 0·65 | 0·72 | 0·73 | 0·62 |
K/Rb | 169·8 | 160·2 | 180·0 | 207·8 | 200·5 | 230·8 | 173·8 | 166·0 | 156·1 | 155·4 | 147·9 | 151·9 | 131·8 | 153·8 | 159·5 | 124·2 | 170·8 | 137·2 |
A/CNK | 0·97 | 1·02 | 1·01 | 1·01 | 0·94 | 0·99 | 1·02 | 0·97 | 0·96 | 0·99 | 1·05 | 1·05 | 0·98 | 0·75 | 0·81 | 0·76 | 0·74 | 1·08 |
Ba | 963 | 1204 | 900 | 928 | 1080 | 1149 | 1181 | 1079 | 1126 | 1115 | 1076 | 1002 | 1084 | 2109 | 1797 | 1578 | 2084 | 901 |
Rb | 199 | 185 | 190 | 175 | 147 | 132 | 170 | 290 | 311 | 304 | 311 | 293 | 354 | 360 | 355 | 409 | 350 | 320 |
Sr | 333 | 413 | 348 | 338 | 361 | 412 | 368 | 318 | 354 | 358 | 312 | 312 | 302 | 495 | 418 | 355 | 350 | 378 |
Zr | 177 | 188 | 171 | 149 | 169 | 226 | 146 | 237 | 283 | 269 | 256 | 259 | 229 | 405 | 390 | 372 | 544 | 240 |
Nb | 12 | 12 | 13 | 18 | 14 | 9 | 14 | 14 | 16 | 17 | 20 | 16 | 19 | 23 | 13 | 20 | — | 21 |
Ga | 21 | 23 | 19 | 20 | b.d. | 23 | 22 | 20 | 20 | 20 | 19 | 18 | 19 | 20 | 19 | 18 | 18 | 24 |
Cr | 61 | 111 | 50 | 54 | 114 | 75 | 131 | 168 | 160 | 132 | 166 | 122 | 157 | 498 | 425 | 504 | 486 | 43 |
Ni | 18 | 25 | 15 | 16 | 31 | 24 | 38 | 33 | 24 | 26 | 30 | 27 | 45 | 135 | 59 | 235 | 127 | 11 |
Co | 8 | 11 | 10 | 7 | 12 | 15 | 16 | 10 | 12 | 12 | 8 | 5 | 12 | 28 | 22 | 28 | 30 | b.d. |
Pb | 40 | 24 | 41 | 43 | 24 | 17 | 34 | 53 | 70 | 68 | 68 | 63 | 60 | 34 | 46 | 53 | 69 | 66 |
Zn | 63 | 79 | 58 | 54 | 51 | 74 | 84 | 55 | 58 | 50 | 53 | 52 | 62 | 85 | 76 | 79 | 70 | 34 |
La | — | 55·2 | 39·8 | 33·1 | 42·9 | 45·6 | — | 109·3 | 43·9 | — | 44·2 | — | 44·5 | 44·8 | 54·0 | 52·6 | — | 18·2 |
Ce | — | 111·1 | 80·9 | 66·2 | 94·6 | 99·6 | — | — | 91·8 | — | 92·3 | — | 96·8 | 110·2 | 125·3 | 119·1 | — | 35·4 |
Pr | — | 12·7 | 9·6 | 8·0 | 11·9 | 12·4 | — | 20·6 | 11·5 | — | 11·7 | — | 11·5 | 15·5 | 17·0 | 15·8 | — | 4·2 |
Nd | — | 42·5 | 31·6 | 26·7 | 43·3 | 44·9 | — | 63·0 | 40·8 | — | 42·1 | — | 39·9 | 61·7 | 62·8 | 58·8 | — | 15·2 |
Sm | — | 7·2 | 5·6 | 5·5 | 9·4 | 9·8 | — | 10·4 | 8·4 | — | 8·8 | — | 8·3 | 14·6 | 13·7 | 13·8 | — | 2·9 |
Eu | — | 1·7 | 1·2 | 1·2 | 1·9 | 1·7 | — | 2·1 | 1·7 | — | 1·8 | — | 1·7 | 3·5 | 2·9 | 3·4 | — | 0·7 |
Gd | — | 5·9 | 4·7 | 4·7 | 8·2 | 9·2 | — | 12·4 | 6·2 | — | 6·4 | — | 6·6 | 10·7 | 10·7 | 10·0 | — | 2·1 |
Tb | — | 0·7 | 0·6 | 0·7 | 1·2 | 1·2 | — | 1·1 | 0·8 | — | 0·9 | — | 0·8 | 1·2 | 1·2 | 1·1 | — | 0·3 |
Dy | — | 3·4 | 3·1 | 3·4 | 5·8 | 6·6 | — | 4·5 | 3·9 | — | 4·1 | — | 4·0 | 5·8 | 5·9 | 5·1 | — | 1·3 |
Ho | — | 0·5 | 0·5 | 0·6 | 1·1 | 1·2 | — | 0·7 | 0·7 | — | 0·7 | — | 0·6 | 0·9 | 1·0 | 0·8 | — | 0·2 |
Er | — | 1·4 | 1·6 | 1·8 | 2·9 | 3·2 | — | 2·0 | 1·9 | — | 2·0 | — | 1·7 | 2·5 | 2·6 | 2·3 | — | 0·6 |
Tm | — | 0·2 | 0·3 | 0·3 | 0·5 | 0·4 | — | 0·3 | 0·3 | — | 0·3 | — | 0·2 | 0·3 | 0·3 | 0·3 | — | 0·1 |
Yb | — | 1·2 | 1·8 | 1·8 | 2·7 | 2·6 | — | 1·9 | 1·7 | — | 1·9 | — | 1·6 | 2·1 | 2·1 | 1·9 | — | 0·6 |
Lu | — | 0·2 | 0·3 | 0·3 | 0·4 | 0·3 | — | 0·3 | 0·3 | — | 0·3 | — | 0·2 | 0·3 | 0·3 | 0·3 | — | 0·1 |
∑REE | — | 244·0 | 181·7 | 154·0 | 226·7 | 238·5 | — | — | 213·9 | — | 217·4 | — | 218·6 | 274·2 | 299·9 | 285·3 | — | 81·9 |
Eu/Eu* | — | 0·8 | 0·7 | 0·7 | 0·7 | 0·5 | — | 0·6 | 0·7 | — | 0·7 | — | 0·7 | 0·8 | 0·7 | 0·9 | — | 0·9 |
CeN/YbN | — | 23·2 | 11·5 | 9·8 | 9·2 | 10·1 | — | — | 13·7 | — | 12·7 | — | 15·7 | 13·6 | 15·5 | 16·0 | — | 15·0 |
Cs | — | 12·2 | 18·8 | 17·4 | 8·5 | 6·4 | — | 30·0 | 51·6 | — | 31·7 | — | 48·9 | 27·0 | 23·7 | 55·5 | — | 66·0 |
Ta | — | 1·4 | 1·4 | 1·7 | 1·5 | 1·0 | — | 2·4 | 2·9 | — | 2·4 | — | 4·4 | 1·8 | 1·7 | 2·2 | — | 2·3 |
Hf | — | 3·8 | 6·3 | 9·9 | 4·5 | 3·3 | — | 6·7 | 8·5 | — | 9·1 | — | 6·7 | 12·8 | 4·3 | 10·8 | — | 8·8 |
The XRF analyses (most major elements, all trace elements Ba–Zn) were carried out using a Philips PW 1450/20 automatic sequential XRF spectrometer at the University of Glasgow. Ferrous iron was determined by potassium dichromate titration with 0·2% solution of sodium diphenylamine sulphonate as an indicator (Pratt, 1894) following a combined H2SO4–HNO3–HF acid attack. The REE were analysed using a VG Plasma Quad PQ1, and Cs, Ta and Hf using a VG Plasma Quad PQ2 Turbo Plus ICP-MS; analyses were carried out at SURRC, East Kilbride, UK. Full analytical details and precise sample location have been given by Janoušek (1994). Major-element analyses shown in italics were carried out using standard methods of wet chemistry in the laboratories of the Czech Geological Survey, Prague.
Sázava suite
Sázava intrusion: 1, biotite–amphibole quartz diorite, Mrac, quarry; 2, biotite–amphibole tonalite, Teletín, disused quarry; 3, biotite–amphibole quartz diorite, Prosecnice, quarry. Basic rocks: 4, biotite–amphibole quartz diorite, Teletín, disused quarry; 5, amphibole–biotite quartz gabbrodiorite, Vavretice. Požáry intrusion: 6, biotite trondhjemite, Krhanice, quarry; 7, biotite trondhjemite, Prosecnice, quarry.
Blatná suite
Kozárovice intrusion: 8, biotite–amphibole granodiorite, Kozárovice, quarry; 9, amphibole–biotite granodiorite, Kozárovice, quarry; 10, porphyritic amphibole–biotite granodiorite, Kozárovice, disused quarry; 11, biotite–amphibole granodiorite, Hrímezdice, disused quarry; 12, porphyritic amphibole–biotite granodiorite (’Technice type’), Kamýk nad Vltavou, rock outcrop. Monzonitic rocks: 13, biotite–amphibole quartz monzonite, Kozárovice, quarry; 14, pyroxene–biotite–amphibole quartz monzonite, Zaluzany, disused quarry; 15, pyroxene–biotite–amphibole monzonite, Luckovice, disused quarry; 16, (pyroxene–) biotite–amphibole monzonite, Luckovice, disused quarry. Blatná intrusion: 17, (amphibole–) biotite granodiorite, Řečice, quarry; 18, (amphibole–) biotite granodiorite, Tuzice, quarry; 19, biotite granodiorite, Paštiky, disused quarry; 20, biotite granodiorite, Defurovy Lazany, quarry; 21, amphibole–biotite granodiorite, Hudcice, quarry; 22, amphibole–biotite granodiorite (’Červená type’), Vlckovice, quarry; 23, amphibole–biotite granodiorite (’Červená type’), Horazd’ovice, quarry.
Čertovo břemeno suite
Sedlčany intrusion: 24, (amphibole–) biotite granite, Vrchotovy Janovice, quarry; 25, amphibole–biotite granite, Vápenice, quarry; 26, biotite granite, Kosova Hora, quarry; 27, amphibole–biotite granite, Vrchotovy Janovice, quarry. Čertovo břemeno intrusion: 28, porphyritic biotite–amphibole syenite, Chyšky, well at water tower (elevation 685 m). Tábor intrusion: 29, pyroxene–biotite quartz syenite, Tábor-Klokoty, disused quarry; 30, minette, Kozlí, quarry; 31, minette, Zalužany, disused quarry.
Říčany suite
Říčany intrusion:32, porphyritic (muscovite)–biotite granite, Zernovka, quarry. Additional analyses for the Říčany suite were given elsewhere (Janoušek et al., 1997c).
qtzd, quartz diorite; gbd, gabbrodiorite.
Sázava suite | Blatná suite | |||||||||||||||||
Intrusion: | Sázava | Teletín | gbd | Požáry | Kozárovice | monzonitic rocks | ||||||||||||
qtzd | ||||||||||||||||||
Sample: | Sa-1 | Sa-4 | Sa-7 | Sa-11 | SaD-1 | Gbs-2 | Po-1 | Po-4 | Koz-2 | Koz-4 | Koz-5 | Koz-6 | Koz-9 | Koz-12 | KozD-1 | Zal-1 | Gbl-1 | Gbl-2 |
Locality: | 1 | 1 | 2 | 3 | 4 | 5 | 6 | 7 | 8 | 9 | 9 | 10 | 11 | 12 | 13 | 14 | 15 | 16 |
SiO2 | 59·98 | 50·72 | 57·73 | 63·72 | 52·90 | 48·84 | 62·95 | 71·09 | 62·92 | 64·79 | 65·53 | 62·59 | 57·69 | 64·60 | 59·58 | 54·22 | 49·21 | 49·62 |
TiO2 | 0·63 | 0·83 | 0·95 | 0·53 | 1·35 | 0·34 | 0·28 | 0·30 | 0·61 | 0·52 | 0·45 | 0·67 | 0·79 | 0·57 | 0·72 | 0·96 | 1·02 | 0·60 |
Al2O3 | 16·42 | 17·57 | 18·82 | 15·63 | 18·23 | 21·64 | 20·02 | 15·09 | 15·69 | 15·28 | 15·43 | 15·66 | 15·81 | 14·99 | 14·80 | 15·24 | 13·69 | 9·06 |
Fe2O3 | 1·35 | 2·19 | 1·00 | 1·31 | 1·47 | 3·28 | 0·67 | 0·38 | 0·86 | 0·96 | 1·46 | 1·08 | 2·11 | 1·27 | 1·69 | 1·17 | 2·47 | 1·64 |
FeO | 5·46 | 7·65 | 5·43 | 4·44 | 7·24 | 2·74 | 1·65 | 2·12 | 3·51 | 2·95 | 2·34 | 3·91 | 4·07 | 2·79 | 4·08 | 6·12 | 6·96 | 6·49 |
MnO | 0·19 | 0·24 | 0·12 | 0·14 | 0·16 | 0·13 | 0·05 | 0·06 | 0·10 | 0·08 | 0·09 | 0·09 | 0·13 | 0·08 | 0·14 | 0·15 | 0·15 | 0·15 |
MgO | 3·21 | 5·18 | 2·82 | 2·13 | 3·89 | 5·11 | 0·55 | 0·52 | 2·96 | 2·33 | 2·14 | 2·72 | 4·70 | 2·37 | 4·11 | 4·94 | 8·53 | 15·07 |
CaO | 7·04 | 9·92 | 7·47 | 5·24 | 8·55 | 13·75 | 6·61 | 3·75 | 4·65 | 4·10 | 3·76 | 4·54 | 5·39 | 3·44 | 5·33 | 7·17 | 9·74 | 8·83 |
Na2O | 2·52 | 2·83 | 2·54 | 3·38 | 2·76 | 1·78 | 3·91 | 3·68 | 3·30 | 3·07 | 3·25 | 2·97 | 3·15 | 3·12 | 2·84 | 2·44 | 1·89 | 1·02 |
K2O | 2·50 | 1·60 | 1·67 | 1·75 | 1·45 | 0·83 | 1·99 | 1·87 | 4·01 | 3·95 | 4·14 | 3·77 | 3·99 | 4·34 | 4·19 | 4·70 | 3·61 | 3·27 |
P2O5 | 0·16 | 0·19 | 0·37 | 0·12 | 0·26 | 0·04 | 0·07 | 0·07 | 0·26 | 0·24 | 0·21 | 0·24 | 0·26 | 0·21 | 0·37 | 0·80 | 0·76 | 0·38 |
H2O+ | 1·18 | 1·17 | 1·14 | 0·87 | 1·53 | 1·57 | 0·71 | 0·71 | 0·88 | 0·80 | 0·72 | 0·97 | 1·02 | 0·97 | 1·34 | 1·48 | 2·05 | 2·55 |
CO2 | 0·18 | 0·09 | 0·13 | 0·34 | 0·06 | 0·51 | 0·35 | 0·27 | 0·13 | 0·03 | 0·06 | 0·05 | 0·26 | 0·21 | 0·19 | 0·05 | 0·16 | 0·11 |
Total | 100·82 | 100·18 | 100·19 | 99·60 | 99·85 | 100·56 | 99·81 | 99·91 | 99·88 | 99·10 | 99·58 | 99·26 | 99·37 | 98·96 | 99·38 | 99·44 | 100·24 | 98·79 |
Mg/(Fe+Mg) | 0·46 | 0·49 | 0·44 | 0·40 | 0·45 | 0·62 | 0·30 | 0·27 | 0·55 | 0·52 | 0·51 | 0·50 | 0·58 | 0·52 | 0·57 | 0·55 | 0·62 | 0·77 |
K/Rb | 273·1 | 237·2 | 243·2 | 227·0 | 279·9 | 222·3 | 323·9 | 267·6 | 232·8 | 204·9 | 197·5 | 230·1 | 188·2 | 208·3 | 186·0 | 176·5 | 194·6 | 158·7 |
A/CNK | 0·84 | 0·72 | 0·96 | 0·92 | 0·84 | 0·75 | 0·97 | 1·01 | 0·86 | 0·91 | 0·93 | 0·91 | 0·82 | 0·93 | 0·78 | 0·69 | 0·55 | 0·43 |
Ba | 1037 | 388 | 722 | 1476 | 1017 | 245 | 1024 | 1284 | 1492 | 1135 | 1286 | 1289 | 1681 | 1154 | 1175 | 2224 | 2329 | 1351 |
Rb | 76 | 56 | 57 | 64 | 43 | 31 | 51 | 58 | 143 | 160 | 174 | 136 | 176 | 173 | 187 | 221 | 154 | 171 |
Sr | 539 | 472 | 537 | 378 | 430 | 278 | 599 | 430 | 500 | 430 | 418 | 409 | 519 | 385 | 379 | 510 | 540 | 218 |
Zr | 76 | 56 | 57 | 74 | 88 | 27 | 128 | 180 | 216 | 201 | 201 | 218 | 251 | 211 | 146 | 251 | 62 | 77 |
Nb | 6 | 5 | 10 | 5 | 10 | 8 | 5 | 6 | — | — | 14 | 13 | 16 | 11 | 9 | 16 | 11 | 7 |
Ga | 17 | 19 | 20 | 16 | 18 | 14 | 18 | 14 | 18 | 18 | 17 | 20 | 17 | 16 | 20 | 19 | 18 | 14 |
Cr | 29 | 53 | 33 | 50 | 43 | 159 | 15 | 16 | 84 | 99 | 113 | 76 | 147 | 57 | 171 | 198 | 496 | 1283 |
Ni | 10 | b.d. | b.d. | b.d. | b.d. | 13 | b.d. | b.d. | 18 | 20 | 19 | 18 | 28 | 17 | 66 | 17 | 71 | 233 |
Co | 17 | 30 | 13 | 13 | 18 | 23 | b.d. | 4 | 9 | 10 | 13 | 12 | 13 | 12 | 20 | 25 | 37 | 57 |
Pb | 22 | 15 | 13 | 15 | b.d. | 13 | 21 | 29 | 34 | 37 | 46 | 29 | 31 | 36 | 42 | 31 | 19 | 12 |
Zn | 71 | 104 | 50 | 73 | 85 | 51 | 23 | 22 | 52 | 50 | 49 | 60 | 69 | 52 | 85 | 85 | 85 | 59 |
La | — | 21·7 | 20·8 | — | 20·0 | — | 11·6 | 26·2 | 35·0 | — | — | 34·8 | — | 32·7 | 25·9 | 43·9 | 27·7 | 26·0 |
Ce | — | 71·8 | 42·0 | — | 46·8 | — | 18·0 | 39·0 | 64·4 | — | — | 68·3 | — | 58·4 | 58·3 | 94·3 | 60·3 | 54·1 |
Pr | — | 6·9 | 5·0 | — | 6·1 | — | 1·8 | 3·9 | 7·9 | — | — | 8·2 | — | 7·3 | 7·8 | 11·7 | 7·7 | 7·1 |
Nd | — | 29·7 | 17·4 | — | 23·5 | — | 5·4 | 11·5 | 27·5 | — | — | 29·4 | — | 24·9 | 28·6 | 45·5 | 29·2 | 26·0 |
Sm | — | 6·2 | 3·8 | — | 5·9 | — | 1·4 | 1·8 | 5·7 | — | — | 6·0 | — | 4·9 | 5·9 | 10·0 | 7·0 | 6·4 |
Eu | — | 1·5 | 1·8 | — | 2·0 | — | 1·3 | 1·0 | 1·5 | — | — | 1·6 | — | 1·3 | 1·5 | 2·5 | 2·2 | 1·6 |
Gd | — | 6·1 | 3·8 | — | 6·2 | — | 1·1 | 1·4 | 4·7 | — | — | 5·3 | — | 4·3 | 4·9 | 8·4 | 7·0 | 5·8 |
Tb | — | 0·9 | 0·6 | — | 1·0 | — | 0·1 | 0·2 | 0·7 | — | — | 0·8 | — | 0·6 | 0·7 | 1·0 | 0·7 | 0·8 |
Dy | — | 5·8 | 2·7 | — | 5·1 | — | 0·6 | 0·8 | 3·5 | — | — | 4·1 | — | 3·1 | 3·4 | 5·6 | 3·7 | 4·2 |
Ho | — | 1·0 | 0·6 | — | 1·1 | — | 0·1 | 0·1 | 0·6 | — | — | 0·7 | — | 0·6 | 0·6 | 1·0 | 0·7 | 0·8 |
Er | — | 2·8 | 1·6 | — | 2·8 | — | 0·4 | 0·5 | 1·8 | — | — | 2·1 | — | 1·7 | 1·8 | 2·8 | 1·8 | 2·2 |
Tm | — | 0·4 | 0·2 | — | 0·5 | — | 0·1 | 0·1 | 0·3 | — | — | 0·3 | — | 0·2 | 0·3 | 0·4 | 0·2 | 0·3 |
Yb | — | 2·9 | 1·5 | — | 2·7 | — | 0·5 | 0·6 | 1·7 | — | — | 2·0 | — | 1·6 | 1·8 | 2·5 | 1·6 | 2·0 |
Lu | — | 0·4 | 0·2 | — | 0·5 | — | 0·1 | 0·1 | 0·3 | — | — | 0·3 | — | 0·3 | 0·3 | 0·4 | 0·2 | 0·3 |
∑REE | — | 158·2 | 101·9 | — | 124·3 | — | 42·4 | 87·1 | 155·6 | — | — | 164·0 | — | 141·8 | 141·8 | 230·0 | 150·3 | 137·5 |
Eu/Eu* | — | 0·7 | 1·4 | — | 1·0 | — | 3·2 | 2·1 | 0·9 | — | — | 0·8 | — | 0·8 | 0·8 | 0·8 | 1·0 | 0·8 |
CeN/YbN | — | 6·4 | 7·2 | — | 4·5 | — | 9·2 | 16·6 | 9·6 | — | — | 8·9 | — | 9·4 | 8·2 | 9·6 | 9·9 | 7·1 |
Cs | — | 5·7 | 6·6 | — | 2·3 | — | 3·0 | 3·0 | 9·9 | — | — | 6·8 | — | 13·0 | 21·3 | 17·7 | 7·8 | 13·1 |
Ta | — | 0·5 | 0·6 | — | 1·1 | — | 0·3 | 0·2 | 1·2 | — | — | 0·7 | — | 1·1 | 1·5 | 1·1 | 0·7 | 0·8 |
Hf | — | 2·5 | 3·6 | — | 1·8 | — | 4·2 | 5·4 | 5·8 | — | — | 6·1 | — | 7·2 | 4·7 | 13·3 | 4·3 | 5·0 |
Sázava suite | Blatná suite | |||||||||||||||||
Intrusion: | Sázava | Teletín | gbd | Požáry | Kozárovice | monzonitic rocks | ||||||||||||
qtzd | ||||||||||||||||||
Sample: | Sa-1 | Sa-4 | Sa-7 | Sa-11 | SaD-1 | Gbs-2 | Po-1 | Po-4 | Koz-2 | Koz-4 | Koz-5 | Koz-6 | Koz-9 | Koz-12 | KozD-1 | Zal-1 | Gbl-1 | Gbl-2 |
Locality: | 1 | 1 | 2 | 3 | 4 | 5 | 6 | 7 | 8 | 9 | 9 | 10 | 11 | 12 | 13 | 14 | 15 | 16 |
SiO2 | 59·98 | 50·72 | 57·73 | 63·72 | 52·90 | 48·84 | 62·95 | 71·09 | 62·92 | 64·79 | 65·53 | 62·59 | 57·69 | 64·60 | 59·58 | 54·22 | 49·21 | 49·62 |
TiO2 | 0·63 | 0·83 | 0·95 | 0·53 | 1·35 | 0·34 | 0·28 | 0·30 | 0·61 | 0·52 | 0·45 | 0·67 | 0·79 | 0·57 | 0·72 | 0·96 | 1·02 | 0·60 |
Al2O3 | 16·42 | 17·57 | 18·82 | 15·63 | 18·23 | 21·64 | 20·02 | 15·09 | 15·69 | 15·28 | 15·43 | 15·66 | 15·81 | 14·99 | 14·80 | 15·24 | 13·69 | 9·06 |
Fe2O3 | 1·35 | 2·19 | 1·00 | 1·31 | 1·47 | 3·28 | 0·67 | 0·38 | 0·86 | 0·96 | 1·46 | 1·08 | 2·11 | 1·27 | 1·69 | 1·17 | 2·47 | 1·64 |
FeO | 5·46 | 7·65 | 5·43 | 4·44 | 7·24 | 2·74 | 1·65 | 2·12 | 3·51 | 2·95 | 2·34 | 3·91 | 4·07 | 2·79 | 4·08 | 6·12 | 6·96 | 6·49 |
MnO | 0·19 | 0·24 | 0·12 | 0·14 | 0·16 | 0·13 | 0·05 | 0·06 | 0·10 | 0·08 | 0·09 | 0·09 | 0·13 | 0·08 | 0·14 | 0·15 | 0·15 | 0·15 |
MgO | 3·21 | 5·18 | 2·82 | 2·13 | 3·89 | 5·11 | 0·55 | 0·52 | 2·96 | 2·33 | 2·14 | 2·72 | 4·70 | 2·37 | 4·11 | 4·94 | 8·53 | 15·07 |
CaO | 7·04 | 9·92 | 7·47 | 5·24 | 8·55 | 13·75 | 6·61 | 3·75 | 4·65 | 4·10 | 3·76 | 4·54 | 5·39 | 3·44 | 5·33 | 7·17 | 9·74 | 8·83 |
Na2O | 2·52 | 2·83 | 2·54 | 3·38 | 2·76 | 1·78 | 3·91 | 3·68 | 3·30 | 3·07 | 3·25 | 2·97 | 3·15 | 3·12 | 2·84 | 2·44 | 1·89 | 1·02 |
K2O | 2·50 | 1·60 | 1·67 | 1·75 | 1·45 | 0·83 | 1·99 | 1·87 | 4·01 | 3·95 | 4·14 | 3·77 | 3·99 | 4·34 | 4·19 | 4·70 | 3·61 | 3·27 |
P2O5 | 0·16 | 0·19 | 0·37 | 0·12 | 0·26 | 0·04 | 0·07 | 0·07 | 0·26 | 0·24 | 0·21 | 0·24 | 0·26 | 0·21 | 0·37 | 0·80 | 0·76 | 0·38 |
H2O+ | 1·18 | 1·17 | 1·14 | 0·87 | 1·53 | 1·57 | 0·71 | 0·71 | 0·88 | 0·80 | 0·72 | 0·97 | 1·02 | 0·97 | 1·34 | 1·48 | 2·05 | 2·55 |
CO2 | 0·18 | 0·09 | 0·13 | 0·34 | 0·06 | 0·51 | 0·35 | 0·27 | 0·13 | 0·03 | 0·06 | 0·05 | 0·26 | 0·21 | 0·19 | 0·05 | 0·16 | 0·11 |
Total | 100·82 | 100·18 | 100·19 | 99·60 | 99·85 | 100·56 | 99·81 | 99·91 | 99·88 | 99·10 | 99·58 | 99·26 | 99·37 | 98·96 | 99·38 | 99·44 | 100·24 | 98·79 |
Mg/(Fe+Mg) | 0·46 | 0·49 | 0·44 | 0·40 | 0·45 | 0·62 | 0·30 | 0·27 | 0·55 | 0·52 | 0·51 | 0·50 | 0·58 | 0·52 | 0·57 | 0·55 | 0·62 | 0·77 |
K/Rb | 273·1 | 237·2 | 243·2 | 227·0 | 279·9 | 222·3 | 323·9 | 267·6 | 232·8 | 204·9 | 197·5 | 230·1 | 188·2 | 208·3 | 186·0 | 176·5 | 194·6 | 158·7 |
A/CNK | 0·84 | 0·72 | 0·96 | 0·92 | 0·84 | 0·75 | 0·97 | 1·01 | 0·86 | 0·91 | 0·93 | 0·91 | 0·82 | 0·93 | 0·78 | 0·69 | 0·55 | 0·43 |
Ba | 1037 | 388 | 722 | 1476 | 1017 | 245 | 1024 | 1284 | 1492 | 1135 | 1286 | 1289 | 1681 | 1154 | 1175 | 2224 | 2329 | 1351 |
Rb | 76 | 56 | 57 | 64 | 43 | 31 | 51 | 58 | 143 | 160 | 174 | 136 | 176 | 173 | 187 | 221 | 154 | 171 |
Sr | 539 | 472 | 537 | 378 | 430 | 278 | 599 | 430 | 500 | 430 | 418 | 409 | 519 | 385 | 379 | 510 | 540 | 218 |
Zr | 76 | 56 | 57 | 74 | 88 | 27 | 128 | 180 | 216 | 201 | 201 | 218 | 251 | 211 | 146 | 251 | 62 | 77 |
Nb | 6 | 5 | 10 | 5 | 10 | 8 | 5 | 6 | — | — | 14 | 13 | 16 | 11 | 9 | 16 | 11 | 7 |
Ga | 17 | 19 | 20 | 16 | 18 | 14 | 18 | 14 | 18 | 18 | 17 | 20 | 17 | 16 | 20 | 19 | 18 | 14 |
Cr | 29 | 53 | 33 | 50 | 43 | 159 | 15 | 16 | 84 | 99 | 113 | 76 | 147 | 57 | 171 | 198 | 496 | 1283 |
Ni | 10 | b.d. | b.d. | b.d. | b.d. | 13 | b.d. | b.d. | 18 | 20 | 19 | 18 | 28 | 17 | 66 | 17 | 71 | 233 |
Co | 17 | 30 | 13 | 13 | 18 | 23 | b.d. | 4 | 9 | 10 | 13 | 12 | 13 | 12 | 20 | 25 | 37 | 57 |
Pb | 22 | 15 | 13 | 15 | b.d. | 13 | 21 | 29 | 34 | 37 | 46 | 29 | 31 | 36 | 42 | 31 | 19 | 12 |
Zn | 71 | 104 | 50 | 73 | 85 | 51 | 23 | 22 | 52 | 50 | 49 | 60 | 69 | 52 | 85 | 85 | 85 | 59 |
La | — | 21·7 | 20·8 | — | 20·0 | — | 11·6 | 26·2 | 35·0 | — | — | 34·8 | — | 32·7 | 25·9 | 43·9 | 27·7 | 26·0 |
Ce | — | 71·8 | 42·0 | — | 46·8 | — | 18·0 | 39·0 | 64·4 | — | — | 68·3 | — | 58·4 | 58·3 | 94·3 | 60·3 | 54·1 |
Pr | — | 6·9 | 5·0 | — | 6·1 | — | 1·8 | 3·9 | 7·9 | — | — | 8·2 | — | 7·3 | 7·8 | 11·7 | 7·7 | 7·1 |
Nd | — | 29·7 | 17·4 | — | 23·5 | — | 5·4 | 11·5 | 27·5 | — | — | 29·4 | — | 24·9 | 28·6 | 45·5 | 29·2 | 26·0 |
Sm | — | 6·2 | 3·8 | — | 5·9 | — | 1·4 | 1·8 | 5·7 | — | — | 6·0 | — | 4·9 | 5·9 | 10·0 | 7·0 | 6·4 |
Eu | — | 1·5 | 1·8 | — | 2·0 | — | 1·3 | 1·0 | 1·5 | — | — | 1·6 | — | 1·3 | 1·5 | 2·5 | 2·2 | 1·6 |
Gd | — | 6·1 | 3·8 | — | 6·2 | — | 1·1 | 1·4 | 4·7 | — | — | 5·3 | — | 4·3 | 4·9 | 8·4 | 7·0 | 5·8 |
Tb | — | 0·9 | 0·6 | — | 1·0 | — | 0·1 | 0·2 | 0·7 | — | — | 0·8 | — | 0·6 | 0·7 | 1·0 | 0·7 | 0·8 |
Dy | — | 5·8 | 2·7 | — | 5·1 | — | 0·6 | 0·8 | 3·5 | — | — | 4·1 | — | 3·1 | 3·4 | 5·6 | 3·7 | 4·2 |
Ho | — | 1·0 | 0·6 | — | 1·1 | — | 0·1 | 0·1 | 0·6 | — | — | 0·7 | — | 0·6 | 0·6 | 1·0 | 0·7 | 0·8 |
Er | — | 2·8 | 1·6 | — | 2·8 | — | 0·4 | 0·5 | 1·8 | — | — | 2·1 | — | 1·7 | 1·8 | 2·8 | 1·8 | 2·2 |
Tm | — | 0·4 | 0·2 | — | 0·5 | — | 0·1 | 0·1 | 0·3 | — | — | 0·3 | — | 0·2 | 0·3 | 0·4 | 0·2 | 0·3 |
Yb | — | 2·9 | 1·5 | — | 2·7 | — | 0·5 | 0·6 | 1·7 | — | — | 2·0 | — | 1·6 | 1·8 | 2·5 | 1·6 | 2·0 |
Lu | — | 0·4 | 0·2 | — | 0·5 | — | 0·1 | 0·1 | 0·3 | — | — | 0·3 | — | 0·3 | 0·3 | 0·4 | 0·2 | 0·3 |
∑REE | — | 158·2 | 101·9 | — | 124·3 | — | 42·4 | 87·1 | 155·6 | — | — | 164·0 | — | 141·8 | 141·8 | 230·0 | 150·3 | 137·5 |
Eu/Eu* | — | 0·7 | 1·4 | — | 1·0 | — | 3·2 | 2·1 | 0·9 | — | — | 0·8 | — | 0·8 | 0·8 | 0·8 | 1·0 | 0·8 |
CeN/YbN | — | 6·4 | 7·2 | — | 4·5 | — | 9·2 | 16·6 | 9·6 | — | — | 8·9 | — | 9·4 | 8·2 | 9·6 | 9·9 | 7·1 |
Cs | — | 5·7 | 6·6 | — | 2·3 | — | 3·0 | 3·0 | 9·9 | — | — | 6·8 | — | 13·0 | 21·3 | 17·7 | 7·8 | 13·1 |
Ta | — | 0·5 | 0·6 | — | 1·1 | — | 0·3 | 0·2 | 1·2 | — | — | 0·7 | — | 1·1 | 1·5 | 1·1 | 0·7 | 0·8 |
Hf | — | 2·5 | 3·6 | — | 1·8 | — | 4·2 | 5·4 | 5·8 | — | — | 6·1 | — | 7·2 | 4·7 | 13·3 | 4·3 | 5·0 |
Blatná suite | Čertovo břemeno suite | Říčany s. | ||||||||||||||||
Intrusion: | Blatná | Sedlčany | Čert. bř. | Tábor | minettes | Říčany | ||||||||||||
Sample: | Bl-1 | Bl-2 | Bl-4 | Bl-7 | Bl-8 | Cv-1 | Cv-3 | Se-1 | Se-5 | Se-6 | Se-9 | Se-12 | Se-15 | Cb-3 | Ta-1 | Mi-1 | Mi-2 | Ri-1 |
Locality: | 17 | 18 | 19 | 20 | 21 | 22 | 23 | 24 | 25 | 25 | 24 | 26 | 27 | 28 | 29 | 30 | 31 | 32 |
SiO2 | 67·08 | 63·16 | 68·11 | 67·80 | 62·94 | 62·88 | 61·86 | 66·58 | 65·87 | 66·70 | 67·74 | 69·06 | 66·47 | 55·96 | 59·69 | 58·32 | 56·22 | 71·43 |
TiO2 | 0·50 | 0·79 | 0·52 | 0·49 | 0·70 | 0·76 | 0·73 | 0·60 | 0·63 | 0·56 | 0·54 | 0·53 | 0·60 | 1·07 | 0·91 | 0·88 | 1·45 | 0·30 |
Al2O3 | 14·88 | 16·33 | 15·43 | 15·43 | 15·74 | 16·15 | 16·17 | 14·58 | 14·41 | 14·72 | 14·55 | 14·37 | 14·47 | 13·62 | 14·13 | 12·27 | 12·47 | 14·58 |
Fe2O3 | 0·81 | 0·50 | 0·68 | 0·55 | 0·60 | 0·88 | 0·81 | 0·51 | 0·56 | 0·54 | 0·57 | 0·29 | 0·52 | 2·29 | 0·38 | 1·69 | 1·51 | 0·26 |
FeO | 2·43 | 3·82 | 2·19 | 2·24 | 3·92 | 3·90 | 4·18 | 2·55 | 2·53 | 2·33 | 2·53 | 2·43 | 2·66 | 3·56 | 4·51 | 4·11 | 3·97 | 0·99 |
MnO | 0·06 | 0·07 | 0·05 | 0·05 | 0·11 | 0·07 | 0·10 | 0·06 | 0·06 | 0·07 | 0·07 | 0·03 | 0·06 | 0·13 | 0·08 | 0·10 | 0·09 | 0·01 |
MgO | 1·82 | 2·64 | 1·61 | 1·59 | 3·17 | 3·49 | 3·58 | 2·53 | 2·53 | 2·56 | 2·38 | 2·19 | 2·55 | 7·33 | 5·07 | 8·25 | 7·97 | 1·12 |
CaO | 2·76 | 3·62 | 2·82 | 2·70 | 4·31 | 4·44 | 3·98 | 2·36 | 2·37 | 2·35 | 2·24 | 2·06 | 2·39 | 4·11 | 3·72 | 3·60 | 3·83 | 1·27 |
Na2O | 3·64 | 3·36 | 3·45 | 3·40 | 3·08 | 2·62 | 2·94 | 2·69 | 2·63 | 2·70 | 2·32 | 2·53 | 2·68 | 2·16 | 2·07 | 1·83 | 1·34 | 3·32 |
K2O | 4·07 | 3·57 | 4·12 | 4·38 | 3·55 | 3·67 | 3·56 | 5·80 | 5·85 | 5·69 | 5·54 | 5·36 | 5·62 | 6·67 | 6·82 | 6·12 | 7·20 | 5·29 |
P2O5 | 0·17 | 0·29 | 0·17 | 0·17 | 0·24 | 0·28 | 0·26 | 0·36 | 0·38 | 0·33 | 0·33 | 0·29 | 0·36 | 0·89 | 0·67 | 0·66 | 0·89 | 0·17 |
H2O+ | 1·00 | 0·97 | 0·79 | 0·63 | 1·13 | 1·01 | 1·01 | 0·90 | 0·92 | 0·76 | 0·77 | 0·68 | 0·88 | 1·53 | 0·80 | 1·50 | 2·09 | 0·51 |
CO2 | 0·37 | 0·06 | 0·06 | 0·04 | 0·27 | 0·14 | 0·19 | 0·04 | 0·03 | 0·25 | 0·26 | 0·33 | 0·04 | 0·19 | 0·04 | 0·51 | 0·25 | 0·03 |
Total | 99·59 | 99·18 | 100·00 | 99·47 | 99·76 | 100·29 | 99·37 | 99·56 | 98·77 | 99·56 | 99·84 | 100·15 | 99·30 | 99·51 | 98·89 | 99·84 | 99·28 | 99·28 |
Mg/(Fe+Mg) | 0·51 | 0·52 | 0·51 | 0·51 | 0·56 | 0·57 | 0·57 | 0·60 | 0·60 | 0·62 | 0·58 | 0·59 | 0·59 | 0·70 | 0·65 | 0·72 | 0·73 | 0·62 |
K/Rb | 169·8 | 160·2 | 180·0 | 207·8 | 200·5 | 230·8 | 173·8 | 166·0 | 156·1 | 155·4 | 147·9 | 151·9 | 131·8 | 153·8 | 159·5 | 124·2 | 170·8 | 137·2 |
A/CNK | 0·97 | 1·02 | 1·01 | 1·01 | 0·94 | 0·99 | 1·02 | 0·97 | 0·96 | 0·99 | 1·05 | 1·05 | 0·98 | 0·75 | 0·81 | 0·76 | 0·74 | 1·08 |
Ba | 963 | 1204 | 900 | 928 | 1080 | 1149 | 1181 | 1079 | 1126 | 1115 | 1076 | 1002 | 1084 | 2109 | 1797 | 1578 | 2084 | 901 |
Rb | 199 | 185 | 190 | 175 | 147 | 132 | 170 | 290 | 311 | 304 | 311 | 293 | 354 | 360 | 355 | 409 | 350 | 320 |
Sr | 333 | 413 | 348 | 338 | 361 | 412 | 368 | 318 | 354 | 358 | 312 | 312 | 302 | 495 | 418 | 355 | 350 | 378 |
Zr | 177 | 188 | 171 | 149 | 169 | 226 | 146 | 237 | 283 | 269 | 256 | 259 | 229 | 405 | 390 | 372 | 544 | 240 |
Nb | 12 | 12 | 13 | 18 | 14 | 9 | 14 | 14 | 16 | 17 | 20 | 16 | 19 | 23 | 13 | 20 | — | 21 |
Ga | 21 | 23 | 19 | 20 | b.d. | 23 | 22 | 20 | 20 | 20 | 19 | 18 | 19 | 20 | 19 | 18 | 18 | 24 |
Cr | 61 | 111 | 50 | 54 | 114 | 75 | 131 | 168 | 160 | 132 | 166 | 122 | 157 | 498 | 425 | 504 | 486 | 43 |
Ni | 18 | 25 | 15 | 16 | 31 | 24 | 38 | 33 | 24 | 26 | 30 | 27 | 45 | 135 | 59 | 235 | 127 | 11 |
Co | 8 | 11 | 10 | 7 | 12 | 15 | 16 | 10 | 12 | 12 | 8 | 5 | 12 | 28 | 22 | 28 | 30 | b.d. |
Pb | 40 | 24 | 41 | 43 | 24 | 17 | 34 | 53 | 70 | 68 | 68 | 63 | 60 | 34 | 46 | 53 | 69 | 66 |
Zn | 63 | 79 | 58 | 54 | 51 | 74 | 84 | 55 | 58 | 50 | 53 | 52 | 62 | 85 | 76 | 79 | 70 | 34 |
La | — | 55·2 | 39·8 | 33·1 | 42·9 | 45·6 | — | 109·3 | 43·9 | — | 44·2 | — | 44·5 | 44·8 | 54·0 | 52·6 | — | 18·2 |
Ce | — | 111·1 | 80·9 | 66·2 | 94·6 | 99·6 | — | — | 91·8 | — | 92·3 | — | 96·8 | 110·2 | 125·3 | 119·1 | — | 35·4 |
Pr | — | 12·7 | 9·6 | 8·0 | 11·9 | 12·4 | — | 20·6 | 11·5 | — | 11·7 | — | 11·5 | 15·5 | 17·0 | 15·8 | — | 4·2 |
Nd | — | 42·5 | 31·6 | 26·7 | 43·3 | 44·9 | — | 63·0 | 40·8 | — | 42·1 | — | 39·9 | 61·7 | 62·8 | 58·8 | — | 15·2 |
Sm | — | 7·2 | 5·6 | 5·5 | 9·4 | 9·8 | — | 10·4 | 8·4 | — | 8·8 | — | 8·3 | 14·6 | 13·7 | 13·8 | — | 2·9 |
Eu | — | 1·7 | 1·2 | 1·2 | 1·9 | 1·7 | — | 2·1 | 1·7 | — | 1·8 | — | 1·7 | 3·5 | 2·9 | 3·4 | — | 0·7 |
Gd | — | 5·9 | 4·7 | 4·7 | 8·2 | 9·2 | — | 12·4 | 6·2 | — | 6·4 | — | 6·6 | 10·7 | 10·7 | 10·0 | — | 2·1 |
Tb | — | 0·7 | 0·6 | 0·7 | 1·2 | 1·2 | — | 1·1 | 0·8 | — | 0·9 | — | 0·8 | 1·2 | 1·2 | 1·1 | — | 0·3 |
Dy | — | 3·4 | 3·1 | 3·4 | 5·8 | 6·6 | — | 4·5 | 3·9 | — | 4·1 | — | 4·0 | 5·8 | 5·9 | 5·1 | — | 1·3 |
Ho | — | 0·5 | 0·5 | 0·6 | 1·1 | 1·2 | — | 0·7 | 0·7 | — | 0·7 | — | 0·6 | 0·9 | 1·0 | 0·8 | — | 0·2 |
Er | — | 1·4 | 1·6 | 1·8 | 2·9 | 3·2 | — | 2·0 | 1·9 | — | 2·0 | — | 1·7 | 2·5 | 2·6 | 2·3 | — | 0·6 |
Tm | — | 0·2 | 0·3 | 0·3 | 0·5 | 0·4 | — | 0·3 | 0·3 | — | 0·3 | — | 0·2 | 0·3 | 0·3 | 0·3 | — | 0·1 |
Yb | — | 1·2 | 1·8 | 1·8 | 2·7 | 2·6 | — | 1·9 | 1·7 | — | 1·9 | — | 1·6 | 2·1 | 2·1 | 1·9 | — | 0·6 |
Lu | — | 0·2 | 0·3 | 0·3 | 0·4 | 0·3 | — | 0·3 | 0·3 | — | 0·3 | — | 0·2 | 0·3 | 0·3 | 0·3 | — | 0·1 |
∑REE | — | 244·0 | 181·7 | 154·0 | 226·7 | 238·5 | — | — | 213·9 | — | 217·4 | — | 218·6 | 274·2 | 299·9 | 285·3 | — | 81·9 |
Eu/Eu* | — | 0·8 | 0·7 | 0·7 | 0·7 | 0·5 | — | 0·6 | 0·7 | — | 0·7 | — | 0·7 | 0·8 | 0·7 | 0·9 | — | 0·9 |
CeN/YbN | — | 23·2 | 11·5 | 9·8 | 9·2 | 10·1 | — | — | 13·7 | — | 12·7 | — | 15·7 | 13·6 | 15·5 | 16·0 | — | 15·0 |
Cs | — | 12·2 | 18·8 | 17·4 | 8·5 | 6·4 | — | 30·0 | 51·6 | — | 31·7 | — | 48·9 | 27·0 | 23·7 | 55·5 | — | 66·0 |
Ta | — | 1·4 | 1·4 | 1·7 | 1·5 | 1·0 | — | 2·4 | 2·9 | — | 2·4 | — | 4·4 | 1·8 | 1·7 | 2·2 | — | 2·3 |
Hf | — | 3·8 | 6·3 | 9·9 | 4·5 | 3·3 | — | 6·7 | 8·5 | — | 9·1 | — | 6·7 | 12·8 | 4·3 | 10·8 | — | 8·8 |
Blatná suite | Čertovo břemeno suite | Říčany s. | ||||||||||||||||
Intrusion: | Blatná | Sedlčany | Čert. bř. | Tábor | minettes | Říčany | ||||||||||||
Sample: | Bl-1 | Bl-2 | Bl-4 | Bl-7 | Bl-8 | Cv-1 | Cv-3 | Se-1 | Se-5 | Se-6 | Se-9 | Se-12 | Se-15 | Cb-3 | Ta-1 | Mi-1 | Mi-2 | Ri-1 |
Locality: | 17 | 18 | 19 | 20 | 21 | 22 | 23 | 24 | 25 | 25 | 24 | 26 | 27 | 28 | 29 | 30 | 31 | 32 |
SiO2 | 67·08 | 63·16 | 68·11 | 67·80 | 62·94 | 62·88 | 61·86 | 66·58 | 65·87 | 66·70 | 67·74 | 69·06 | 66·47 | 55·96 | 59·69 | 58·32 | 56·22 | 71·43 |
TiO2 | 0·50 | 0·79 | 0·52 | 0·49 | 0·70 | 0·76 | 0·73 | 0·60 | 0·63 | 0·56 | 0·54 | 0·53 | 0·60 | 1·07 | 0·91 | 0·88 | 1·45 | 0·30 |
Al2O3 | 14·88 | 16·33 | 15·43 | 15·43 | 15·74 | 16·15 | 16·17 | 14·58 | 14·41 | 14·72 | 14·55 | 14·37 | 14·47 | 13·62 | 14·13 | 12·27 | 12·47 | 14·58 |
Fe2O3 | 0·81 | 0·50 | 0·68 | 0·55 | 0·60 | 0·88 | 0·81 | 0·51 | 0·56 | 0·54 | 0·57 | 0·29 | 0·52 | 2·29 | 0·38 | 1·69 | 1·51 | 0·26 |
FeO | 2·43 | 3·82 | 2·19 | 2·24 | 3·92 | 3·90 | 4·18 | 2·55 | 2·53 | 2·33 | 2·53 | 2·43 | 2·66 | 3·56 | 4·51 | 4·11 | 3·97 | 0·99 |
MnO | 0·06 | 0·07 | 0·05 | 0·05 | 0·11 | 0·07 | 0·10 | 0·06 | 0·06 | 0·07 | 0·07 | 0·03 | 0·06 | 0·13 | 0·08 | 0·10 | 0·09 | 0·01 |
MgO | 1·82 | 2·64 | 1·61 | 1·59 | 3·17 | 3·49 | 3·58 | 2·53 | 2·53 | 2·56 | 2·38 | 2·19 | 2·55 | 7·33 | 5·07 | 8·25 | 7·97 | 1·12 |
CaO | 2·76 | 3·62 | 2·82 | 2·70 | 4·31 | 4·44 | 3·98 | 2·36 | 2·37 | 2·35 | 2·24 | 2·06 | 2·39 | 4·11 | 3·72 | 3·60 | 3·83 | 1·27 |
Na2O | 3·64 | 3·36 | 3·45 | 3·40 | 3·08 | 2·62 | 2·94 | 2·69 | 2·63 | 2·70 | 2·32 | 2·53 | 2·68 | 2·16 | 2·07 | 1·83 | 1·34 | 3·32 |
K2O | 4·07 | 3·57 | 4·12 | 4·38 | 3·55 | 3·67 | 3·56 | 5·80 | 5·85 | 5·69 | 5·54 | 5·36 | 5·62 | 6·67 | 6·82 | 6·12 | 7·20 | 5·29 |
P2O5 | 0·17 | 0·29 | 0·17 | 0·17 | 0·24 | 0·28 | 0·26 | 0·36 | 0·38 | 0·33 | 0·33 | 0·29 | 0·36 | 0·89 | 0·67 | 0·66 | 0·89 | 0·17 |
H2O+ | 1·00 | 0·97 | 0·79 | 0·63 | 1·13 | 1·01 | 1·01 | 0·90 | 0·92 | 0·76 | 0·77 | 0·68 | 0·88 | 1·53 | 0·80 | 1·50 | 2·09 | 0·51 |
CO2 | 0·37 | 0·06 | 0·06 | 0·04 | 0·27 | 0·14 | 0·19 | 0·04 | 0·03 | 0·25 | 0·26 | 0·33 | 0·04 | 0·19 | 0·04 | 0·51 | 0·25 | 0·03 |
Total | 99·59 | 99·18 | 100·00 | 99·47 | 99·76 | 100·29 | 99·37 | 99·56 | 98·77 | 99·56 | 99·84 | 100·15 | 99·30 | 99·51 | 98·89 | 99·84 | 99·28 | 99·28 |
Mg/(Fe+Mg) | 0·51 | 0·52 | 0·51 | 0·51 | 0·56 | 0·57 | 0·57 | 0·60 | 0·60 | 0·62 | 0·58 | 0·59 | 0·59 | 0·70 | 0·65 | 0·72 | 0·73 | 0·62 |
K/Rb | 169·8 | 160·2 | 180·0 | 207·8 | 200·5 | 230·8 | 173·8 | 166·0 | 156·1 | 155·4 | 147·9 | 151·9 | 131·8 | 153·8 | 159·5 | 124·2 | 170·8 | 137·2 |
A/CNK | 0·97 | 1·02 | 1·01 | 1·01 | 0·94 | 0·99 | 1·02 | 0·97 | 0·96 | 0·99 | 1·05 | 1·05 | 0·98 | 0·75 | 0·81 | 0·76 | 0·74 | 1·08 |
Ba | 963 | 1204 | 900 | 928 | 1080 | 1149 | 1181 | 1079 | 1126 | 1115 | 1076 | 1002 | 1084 | 2109 | 1797 | 1578 | 2084 | 901 |
Rb | 199 | 185 | 190 | 175 | 147 | 132 | 170 | 290 | 311 | 304 | 311 | 293 | 354 | 360 | 355 | 409 | 350 | 320 |
Sr | 333 | 413 | 348 | 338 | 361 | 412 | 368 | 318 | 354 | 358 | 312 | 312 | 302 | 495 | 418 | 355 | 350 | 378 |
Zr | 177 | 188 | 171 | 149 | 169 | 226 | 146 | 237 | 283 | 269 | 256 | 259 | 229 | 405 | 390 | 372 | 544 | 240 |
Nb | 12 | 12 | 13 | 18 | 14 | 9 | 14 | 14 | 16 | 17 | 20 | 16 | 19 | 23 | 13 | 20 | — | 21 |
Ga | 21 | 23 | 19 | 20 | b.d. | 23 | 22 | 20 | 20 | 20 | 19 | 18 | 19 | 20 | 19 | 18 | 18 | 24 |
Cr | 61 | 111 | 50 | 54 | 114 | 75 | 131 | 168 | 160 | 132 | 166 | 122 | 157 | 498 | 425 | 504 | 486 | 43 |
Ni | 18 | 25 | 15 | 16 | 31 | 24 | 38 | 33 | 24 | 26 | 30 | 27 | 45 | 135 | 59 | 235 | 127 | 11 |
Co | 8 | 11 | 10 | 7 | 12 | 15 | 16 | 10 | 12 | 12 | 8 | 5 | 12 | 28 | 22 | 28 | 30 | b.d. |
Pb | 40 | 24 | 41 | 43 | 24 | 17 | 34 | 53 | 70 | 68 | 68 | 63 | 60 | 34 | 46 | 53 | 69 | 66 |
Zn | 63 | 79 | 58 | 54 | 51 | 74 | 84 | 55 | 58 | 50 | 53 | 52 | 62 | 85 | 76 | 79 | 70 | 34 |
La | — | 55·2 | 39·8 | 33·1 | 42·9 | 45·6 | — | 109·3 | 43·9 | — | 44·2 | — | 44·5 | 44·8 | 54·0 | 52·6 | — | 18·2 |
Ce | — | 111·1 | 80·9 | 66·2 | 94·6 | 99·6 | — | — | 91·8 | — | 92·3 | — | 96·8 | 110·2 | 125·3 | 119·1 | — | 35·4 |
Pr | — | 12·7 | 9·6 | 8·0 | 11·9 | 12·4 | — | 20·6 | 11·5 | — | 11·7 | — | 11·5 | 15·5 | 17·0 | 15·8 | — | 4·2 |
Nd | — | 42·5 | 31·6 | 26·7 | 43·3 | 44·9 | — | 63·0 | 40·8 | — | 42·1 | — | 39·9 | 61·7 | 62·8 | 58·8 | — | 15·2 |
Sm | — | 7·2 | 5·6 | 5·5 | 9·4 | 9·8 | — | 10·4 | 8·4 | — | 8·8 | — | 8·3 | 14·6 | 13·7 | 13·8 | — | 2·9 |
Eu | — | 1·7 | 1·2 | 1·2 | 1·9 | 1·7 | — | 2·1 | 1·7 | — | 1·8 | — | 1·7 | 3·5 | 2·9 | 3·4 | — | 0·7 |
Gd | — | 5·9 | 4·7 | 4·7 | 8·2 | 9·2 | — | 12·4 | 6·2 | — | 6·4 | — | 6·6 | 10·7 | 10·7 | 10·0 | — | 2·1 |
Tb | — | 0·7 | 0·6 | 0·7 | 1·2 | 1·2 | — | 1·1 | 0·8 | — | 0·9 | — | 0·8 | 1·2 | 1·2 | 1·1 | — | 0·3 |
Dy | — | 3·4 | 3·1 | 3·4 | 5·8 | 6·6 | — | 4·5 | 3·9 | — | 4·1 | — | 4·0 | 5·8 | 5·9 | 5·1 | — | 1·3 |
Ho | — | 0·5 | 0·5 | 0·6 | 1·1 | 1·2 | — | 0·7 | 0·7 | — | 0·7 | — | 0·6 | 0·9 | 1·0 | 0·8 | — | 0·2 |
Er | — | 1·4 | 1·6 | 1·8 | 2·9 | 3·2 | — | 2·0 | 1·9 | — | 2·0 | — | 1·7 | 2·5 | 2·6 | 2·3 | — | 0·6 |
Tm | — | 0·2 | 0·3 | 0·3 | 0·5 | 0·4 | — | 0·3 | 0·3 | — | 0·3 | — | 0·2 | 0·3 | 0·3 | 0·3 | — | 0·1 |
Yb | — | 1·2 | 1·8 | 1·8 | 2·7 | 2·6 | — | 1·9 | 1·7 | — | 1·9 | — | 1·6 | 2·1 | 2·1 | 1·9 | — | 0·6 |
Lu | — | 0·2 | 0·3 | 0·3 | 0·4 | 0·3 | — | 0·3 | 0·3 | — | 0·3 | — | 0·2 | 0·3 | 0·3 | 0·3 | — | 0·1 |
∑REE | — | 244·0 | 181·7 | 154·0 | 226·7 | 238·5 | — | — | 213·9 | — | 217·4 | — | 218·6 | 274·2 | 299·9 | 285·3 | — | 81·9 |
Eu/Eu* | — | 0·8 | 0·7 | 0·7 | 0·7 | 0·5 | — | 0·6 | 0·7 | — | 0·7 | — | 0·7 | 0·8 | 0·7 | 0·9 | — | 0·9 |
CeN/YbN | — | 23·2 | 11·5 | 9·8 | 9·2 | 10·1 | — | — | 13·7 | — | 12·7 | — | 15·7 | 13·6 | 15·5 | 16·0 | — | 15·0 |
Cs | — | 12·2 | 18·8 | 17·4 | 8·5 | 6·4 | — | 30·0 | 51·6 | — | 31·7 | — | 48·9 | 27·0 | 23·7 | 55·5 | — | 66·0 |
Ta | — | 1·4 | 1·4 | 1·7 | 1·5 | 1·0 | — | 2·4 | 2·9 | — | 2·4 | — | 4·4 | 1·8 | 1·7 | 2·2 | — | 2·3 |
Hf | — | 3·8 | 6·3 | 9·9 | 4·5 | 3·3 | — | 6·7 | 8·5 | — | 9·1 | — | 6·7 | 12·8 | 4·3 | 10·8 | — | 8·8 |
The XRF analyses (most major elements, all trace elements Ba–Zn) were carried out using a Philips PW 1450/20 automatic sequential XRF spectrometer at the University of Glasgow. Ferrous iron was determined by potassium dichromate titration with 0·2% solution of sodium diphenylamine sulphonate as an indicator (Pratt, 1894) following a combined H2SO4–HNO3–HF acid attack. The REE were analysed using a VG Plasma Quad PQ1, and Cs, Ta and Hf using a VG Plasma Quad PQ2 Turbo Plus ICP-MS; analyses were carried out at SURRC, East Kilbride, UK. Full analytical details and precise sample location have been given by Janoušek (1994). Major-element analyses shown in italics were carried out using standard methods of wet chemistry in the laboratories of the Czech Geological Survey, Prague.
Sázava suite
Sázava intrusion: 1, biotite–amphibole quartz diorite, Mrac, quarry; 2, biotite–amphibole tonalite, Teletín, disused quarry; 3, biotite–amphibole quartz diorite, Prosecnice, quarry. Basic rocks: 4, biotite–amphibole quartz diorite, Teletín, disused quarry; 5, amphibole–biotite quartz gabbrodiorite, Vavretice. Požáry intrusion: 6, biotite trondhjemite, Krhanice, quarry; 7, biotite trondhjemite, Prosecnice, quarry.
Blatná suite
Kozárovice intrusion: 8, biotite–amphibole granodiorite, Kozárovice, quarry; 9, amphibole–biotite granodiorite, Kozárovice, quarry; 10, porphyritic amphibole–biotite granodiorite, Kozárovice, disused quarry; 11, biotite–amphibole granodiorite, Hrímezdice, disused quarry; 12, porphyritic amphibole–biotite granodiorite (’Technice type’), Kamýk nad Vltavou, rock outcrop. Monzonitic rocks: 13, biotite–amphibole quartz monzonite, Kozárovice, quarry; 14, pyroxene–biotite–amphibole quartz monzonite, Zaluzany, disused quarry; 15, pyroxene–biotite–amphibole monzonite, Luckovice, disused quarry; 16, (pyroxene–) biotite–amphibole monzonite, Luckovice, disused quarry. Blatná intrusion: 17, (amphibole–) biotite granodiorite, Řečice, quarry; 18, (amphibole–) biotite granodiorite, Tuzice, quarry; 19, biotite granodiorite, Paštiky, disused quarry; 20, biotite granodiorite, Defurovy Lazany, quarry; 21, amphibole–biotite granodiorite, Hudcice, quarry; 22, amphibole–biotite granodiorite (’Červená type’), Vlckovice, quarry; 23, amphibole–biotite granodiorite (’Červená type’), Horazd’ovice, quarry.
Čertovo břemeno suite
Sedlčany intrusion: 24, (amphibole–) biotite granite, Vrchotovy Janovice, quarry; 25, amphibole–biotite granite, Vápenice, quarry; 26, biotite granite, Kosova Hora, quarry; 27, amphibole–biotite granite, Vrchotovy Janovice, quarry. Čertovo břemeno intrusion: 28, porphyritic biotite–amphibole syenite, Chyšky, well at water tower (elevation 685 m). Tábor intrusion: 29, pyroxene–biotite quartz syenite, Tábor-Klokoty, disused quarry; 30, minette, Kozlí, quarry; 31, minette, Zalužany, disused quarry.
Říčany suite
Říčany intrusion:32, porphyritic (muscovite)–biotite granite, Zernovka, quarry. Additional analyses for the Říčany suite were given elsewhere (Janoušek et al., 1997c).
qtzd, quartz diorite; gbd, gabbrodiorite.
Trace elements
The granitoids of the CBP show a progressive increase in K2O and Rb and decrease in K/Rb from Sázava to the Blatná, Čertovo břemeno and Říčany suites (Fig. 4; Table 1). The Sázava and Blatná suites have also lower Cs concentrations than both the Čertovo břemeno and Říčany suites.
Compared with the other suites within the CBP, the granitoids of the Sázava suite have low contents of high field strength elements (HFSE), except for Y (Fig. 4a). Such depletions are considered to be typical of subduction settings (e.g. Pearce et al., 1984; Saunders et al., 1991). This suite, including its more basic members, also has low contents of transition metals, particularly Cr and Ni, probably as a result of extensive fractionation. Chondrite-normalized rare earth element (REE) patterns for the majority of the suite are slightly light REE (LREE) enriched with CeN/YbN = 4·5–7·2, whereas those of the Požáry trondhjemites are U-shaped (Fig. 5a). The trondhjemites have total REE contents about half of those in the Sázava intrusion with a significantly higher LREE/HREE (heavy REE) ratio. The magnitude of the Eu anomaly is extremely variable, ranging from negative (Eu/Eu* = 0·7; Sázava tonalite) to positive (up to Eu/Eu* = 3·2; Požáry trondhjemite).
The Blatná suite has higher HFSE concentrations, although there is some overlap with the Sázava suite (Fig. 4b). The concentrations of Cr, Ni and Co are generally comparable, but somewhat higher in some of the monzonitic rocks. The REE patterns are steeper (CeN/YbN = 7·2–23·2) with moderate negative Eu anomalies (Eu/Eu* = 0·9–0·5) (Fig. 5b, c), except for monzonite Gbl-1 (Table 1).
The Čertovo břemeno suite has the highest HFSE concentrations, particularly of Zr, but Y is similar to the Sázava and Blatná suites (Fig. 4c). The suite typically has high contents of Cr and Ni, whereas Co is somewhat lower than in the Sázava suite (Table 1). The Čertovo břemeno suite is characterized by the highest ∑REE accompanied by high LREE/HREE ratios (CeN/YbN = 12·7–16·0) (Fig. 5d, e). All samples have negative Eu anomalies (Eu/Eu* = 0·6–0·9), with patterns of the mafic Čertovo břemeno intrusion and a minette nearly identical (Fig. 5d). The Tábor biotitite studied by Bowes & Košler (1993) is unusual in having a very pronounced negative Eu anomaly (Eu/Eu* = 0·3) and high ∑REE (Fig. 5e).
The trace-element geochemistry of the Říčany suite has been discussed by Janoušek et al. (1997c). In summary, the HFSE content in the Říčany granite is generally transitional between that of the Blatná and Čertovo břemeno suites although its Y is significantly lower (Fig. 4d). This suite is poor in all transition metals. The ∑REE is low and chondrite-normalized patterns are characterized by a strong LREE/HREE enrichment (CeN/YbN = 15–20) (Fig. 5f). The Říčany granite has a variable negative Eu anomaly and low contents of HREE. A sample of the late-stage leucogranite has low ∑REE = 55 and a slight positive Eu anomaly (Eu/Eu* = 1·2).
Sr–Nd isotope geochemistry
On the basis of the whole-rock Sr–Nd isotope geochemistry given by Janoušek et al. (1995), the earlier intrusions (Sázava suite) have Sr–Nd isotopic compositions close to Bulk Earth at 350 Ma, whereas the later intrusions shift towards more radiogenic Sr and less radiogenic Nd signatures (Říčany and Čertovo břemeno suites) (Fig. 6; Table 2). Overall, the isotopic data show a broad negative correlation with the total range of (87Sr/86Sr)350 = 0·7050–0·7120 and εNd350 = +0·4 to −8·7 (Table 2). As demonstrated by Janoušek et al. (1995,1997b) and below, this cannot be interpreted as a simple contamination trend, but it reflects major differences in sources and processes involved in genesis of particular granitoid suites and intrusions.
Sázava suite | Blatná suite | ||||||||||
Intrusion: | Sázava | Kozárovice | Blatná | monzonitic rocks | |||||||
Sa-1 | Sa-3 | Koz-2 | Koz-4 | Koz-5 | Koz-6 | Koz-12 | Bl-2 | Cv-1 | Gbl-1 | Gbl-2 | |
Rb (ppm) | 76 | 55 | 164·1 | 174·5 | 181·9 | 146·7 | 172·9 | 185 | 132 | 138·2 | 171 |
Sr (ppm) | 555·8 | 606·1 | 486·9 | 437·6 | 410·3 | 417·7 | 398·5 | 439·1 | 404·6 | 547·5 | 221·3 |
87Rb/86Sr | 0·3955 | 0·2627 | 0·9767 | 1·1544 | 1·2838 | 1·0167 | 1·2564 | 1·2189 | 0·9438 | 0·7305 | 2·2389 |
87Sr/86Sr | 0·70700(3) | 0·70638(3) | 0·71258(4) | 0·71367(3) | 0·71434(4) | 0·71209(3) | 0·71373(4) | 0·71434(3) | 0·71362(4) | 0·71114(4) | 0·71863(4) |
87Sr/86Sr350 | 0·70503 | 0·70507 | 0·70771 | 0·70792 | 0·70794 | 0·70703 | 0·70747 | 0·70827 | 0·70891 | 0·70750 | 0·70747 |
Sm (ppm) | 4·57 | 6·66 | 5·91 | 5·36 | 5·04 | 6·23 | — | 6·85 | 10·83 | 6·39 | 6·09 |
Nd (ppm) | 24·2 | 33·9 | 31·7 | 28·9 | 26·7 | 33·4 | — | 43·8 | 50·1 | 31·7 | 26·9 |
147Sm/144Nd | 0·1188 | 0·1189 | 0·1128 | 0·1121 | 0·1141 | 0·1127 | — | 0·0946 | 0·1307 | 0·1217 | 0·1366 |
143Nd/144Nd | 0·512476(6) | 0·512479(7) | 0·512210(7) | 0·512186(5) | 0·512187(7) | 0·512267(7) | — | 0·512101(7) | 0·512225(6) | 0·512316 | 0·512334(7) |
143Nd/144Nd350 | 0·512204 | 0·512207 | 0·511952 | 0·511929 | 0·511926 | 0·512009 | — | 0·511884 | 0·511925 | 0·512037 | 0·512021 |
εNd350 | 0·3 | 0·4 | −4·6 | −5·0 | −5·1 | −3·5 | — | −5·9 | −5·1 | −2·9 | −3·2 |
Sázava suite | Blatná suite | ||||||||||
Intrusion: | Sázava | Kozárovice | Blatná | monzonitic rocks | |||||||
Sa-1 | Sa-3 | Koz-2 | Koz-4 | Koz-5 | Koz-6 | Koz-12 | Bl-2 | Cv-1 | Gbl-1 | Gbl-2 | |
Rb (ppm) | 76 | 55 | 164·1 | 174·5 | 181·9 | 146·7 | 172·9 | 185 | 132 | 138·2 | 171 |
Sr (ppm) | 555·8 | 606·1 | 486·9 | 437·6 | 410·3 | 417·7 | 398·5 | 439·1 | 404·6 | 547·5 | 221·3 |
87Rb/86Sr | 0·3955 | 0·2627 | 0·9767 | 1·1544 | 1·2838 | 1·0167 | 1·2564 | 1·2189 | 0·9438 | 0·7305 | 2·2389 |
87Sr/86Sr | 0·70700(3) | 0·70638(3) | 0·71258(4) | 0·71367(3) | 0·71434(4) | 0·71209(3) | 0·71373(4) | 0·71434(3) | 0·71362(4) | 0·71114(4) | 0·71863(4) |
87Sr/86Sr350 | 0·70503 | 0·70507 | 0·70771 | 0·70792 | 0·70794 | 0·70703 | 0·70747 | 0·70827 | 0·70891 | 0·70750 | 0·70747 |
Sm (ppm) | 4·57 | 6·66 | 5·91 | 5·36 | 5·04 | 6·23 | — | 6·85 | 10·83 | 6·39 | 6·09 |
Nd (ppm) | 24·2 | 33·9 | 31·7 | 28·9 | 26·7 | 33·4 | — | 43·8 | 50·1 | 31·7 | 26·9 |
147Sm/144Nd | 0·1188 | 0·1189 | 0·1128 | 0·1121 | 0·1141 | 0·1127 | — | 0·0946 | 0·1307 | 0·1217 | 0·1366 |
143Nd/144Nd | 0·512476(6) | 0·512479(7) | 0·512210(7) | 0·512186(5) | 0·512187(7) | 0·512267(7) | — | 0·512101(7) | 0·512225(6) | 0·512316 | 0·512334(7) |
143Nd/144Nd350 | 0·512204 | 0·512207 | 0·511952 | 0·511929 | 0·511926 | 0·512009 | — | 0·511884 | 0·511925 | 0·512037 | 0·512021 |
εNd350 | 0·3 | 0·4 | −4·6 | −5·0 | −5·1 | −3·5 | — | −5·9 | −5·1 | −2·9 | −3·2 |
Čertovo břemeno suite | Říčany suite | ||||||||||
Intrusion: | Sedlčany | minettes | Říčany | ||||||||
Se-1 | Se-5 | Se-9 | Mi-2 | Mi-1 | Ri-1 | Ri-2 | Ri-4 | Ri-5 | Ri-6 | Ri-10 | |
Rb (ppm) | 310·9 | 314·4 | 308·1 | 350 | 421·8 | 310·7 | 326·9 | 319·2 | 310·4 | 317·3 | 322·9 |
Sr (ppm) | 313·9 | 339 | 307·8 | 333·7 | 354·1 | 374·1 | 360·2 | 377·7 | 399·5 | 386·6 | 322·4 |
87Rb/86Sr | 2·8703 | 2·6879 | 2·9016 | 3·0408 | 3·4540 | 2·4058 | 2·6299 | 2·4483 | 2·2510 | 2·3776 | 2·9034 |
87Sr/86Sr | 0·72615(3) | 0·72543(3) | 0·72620(3) | 0·72700(4) | 0·72907(4) | 0·72154(3) | 0·72267(3) | 0·72216(4) | 0·72134(4) | 0·72186(3) | 0·72431(3) |
87Sr/86Sr350 | 0·71185 | 0·71204 | 0·71174 | 0·71185 | 0·71187 | 0·70955 | 0·70956 | 0·70996 | 0·71013 | 0·71001 | 0·70984 |
Sm (ppm) | 8·26 | 7·88 | 8·17 | 16·25 | 12·60 | 4·06 | 4·98 | 4·59 | 3·83 | 4·56 | 4·40 |
Nd (ppm) | 40·0 | 40·2 | 40·2 | 75·9 | 61·7 | 24·1 | 29·0 | 27·9 | 23·6 | 28·1 | 26·5 |
147Sm/144Nd | 0·1253 | 0·1186 | 0·1228 | 0·1293 | 0·1235 | 0·1020 | 0·1005 | 0·0995 | 0·0980 | 0·0980 | 0·1005 |
143Nd/144Nd | 0·512114(7) | 0·512103(8) | 0·512080(10) | 0·512140(7) | 0·512113(7) | 0·512053(6) | 0·512035(6) | 0·512062(11) | 0·512074(14) | 0·512068(7) | 0·512075(9) |
143Nd/144Nd350 | 0·511827 | 0·511831 | 0·511799 | 0·511844 | 0·51183 | 0·511819 | 0·511805 | 0·511834 | 0·511849 | 0·511843 | 0·511845 |
εNd350 | −7·0 | −7·0 | −7·6 | −6·7 | −7·0 | −7·2 | −7·5 | −6·9 | −6·6 | −6·7 | −6·7 |
Čertovo břemeno suite | Říčany suite | ||||||||||
Intrusion: | Sedlčany | minettes | Říčany | ||||||||
Se-1 | Se-5 | Se-9 | Mi-2 | Mi-1 | Ri-1 | Ri-2 | Ri-4 | Ri-5 | Ri-6 | Ri-10 | |
Rb (ppm) | 310·9 | 314·4 | 308·1 | 350 | 421·8 | 310·7 | 326·9 | 319·2 | 310·4 | 317·3 | 322·9 |
Sr (ppm) | 313·9 | 339 | 307·8 | 333·7 | 354·1 | 374·1 | 360·2 | 377·7 | 399·5 | 386·6 | 322·4 |
87Rb/86Sr | 2·8703 | 2·6879 | 2·9016 | 3·0408 | 3·4540 | 2·4058 | 2·6299 | 2·4483 | 2·2510 | 2·3776 | 2·9034 |
87Sr/86Sr | 0·72615(3) | 0·72543(3) | 0·72620(3) | 0·72700(4) | 0·72907(4) | 0·72154(3) | 0·72267(3) | 0·72216(4) | 0·72134(4) | 0·72186(3) | 0·72431(3) |
87Sr/86Sr350 | 0·71185 | 0·71204 | 0·71174 | 0·71185 | 0·71187 | 0·70955 | 0·70956 | 0·70996 | 0·71013 | 0·71001 | 0·70984 |
Sm (ppm) | 8·26 | 7·88 | 8·17 | 16·25 | 12·60 | 4·06 | 4·98 | 4·59 | 3·83 | 4·56 | 4·40 |
Nd (ppm) | 40·0 | 40·2 | 40·2 | 75·9 | 61·7 | 24·1 | 29·0 | 27·9 | 23·6 | 28·1 | 26·5 |
147Sm/144Nd | 0·1253 | 0·1186 | 0·1228 | 0·1293 | 0·1235 | 0·1020 | 0·1005 | 0·0995 | 0·0980 | 0·0980 | 0·1005 |
143Nd/144Nd | 0·512114(7) | 0·512103(8) | 0·512080(10) | 0·512140(7) | 0·512113(7) | 0·512053(6) | 0·512035(6) | 0·512062(11) | 0·512074(14) | 0·512068(7) | 0·512075(9) |
143Nd/144Nd350 | 0·511827 | 0·511831 | 0·511799 | 0·511844 | 0·51183 | 0·511819 | 0·511805 | 0·511834 | 0·511849 | 0·511843 | 0·511845 |
εNd350 | −7·0 | −7·0 | −7·6 | −6·7 | −7·0 | −7·2 | −7·5 | −6·9 | −6·6 | −6·7 | −6·7 |
Analytical details have been given by Janoušek et al. (1995); sample descriptions and locations are given in Table 1 and by Janoušek et al. (1995); errors in parentheses are 2 SE.
Sázava suite | Blatná suite | ||||||||||
Intrusion: | Sázava | Kozárovice | Blatná | monzonitic rocks | |||||||
Sa-1 | Sa-3 | Koz-2 | Koz-4 | Koz-5 | Koz-6 | Koz-12 | Bl-2 | Cv-1 | Gbl-1 | Gbl-2 | |
Rb (ppm) | 76 | 55 | 164·1 | 174·5 | 181·9 | 146·7 | 172·9 | 185 | 132 | 138·2 | 171 |
Sr (ppm) | 555·8 | 606·1 | 486·9 | 437·6 | 410·3 | 417·7 | 398·5 | 439·1 | 404·6 | 547·5 | 221·3 |
87Rb/86Sr | 0·3955 | 0·2627 | 0·9767 | 1·1544 | 1·2838 | 1·0167 | 1·2564 | 1·2189 | 0·9438 | 0·7305 | 2·2389 |
87Sr/86Sr | 0·70700(3) | 0·70638(3) | 0·71258(4) | 0·71367(3) | 0·71434(4) | 0·71209(3) | 0·71373(4) | 0·71434(3) | 0·71362(4) | 0·71114(4) | 0·71863(4) |
87Sr/86Sr350 | 0·70503 | 0·70507 | 0·70771 | 0·70792 | 0·70794 | 0·70703 | 0·70747 | 0·70827 | 0·70891 | 0·70750 | 0·70747 |
Sm (ppm) | 4·57 | 6·66 | 5·91 | 5·36 | 5·04 | 6·23 | — | 6·85 | 10·83 | 6·39 | 6·09 |
Nd (ppm) | 24·2 | 33·9 | 31·7 | 28·9 | 26·7 | 33·4 | — | 43·8 | 50·1 | 31·7 | 26·9 |
147Sm/144Nd | 0·1188 | 0·1189 | 0·1128 | 0·1121 | 0·1141 | 0·1127 | — | 0·0946 | 0·1307 | 0·1217 | 0·1366 |
143Nd/144Nd | 0·512476(6) | 0·512479(7) | 0·512210(7) | 0·512186(5) | 0·512187(7) | 0·512267(7) | — | 0·512101(7) | 0·512225(6) | 0·512316 | 0·512334(7) |
143Nd/144Nd350 | 0·512204 | 0·512207 | 0·511952 | 0·511929 | 0·511926 | 0·512009 | — | 0·511884 | 0·511925 | 0·512037 | 0·512021 |
εNd350 | 0·3 | 0·4 | −4·6 | −5·0 | −5·1 | −3·5 | — | −5·9 | −5·1 | −2·9 | −3·2 |
Sázava suite | Blatná suite | ||||||||||
Intrusion: | Sázava | Kozárovice | Blatná | monzonitic rocks | |||||||
Sa-1 | Sa-3 | Koz-2 | Koz-4 | Koz-5 | Koz-6 | Koz-12 | Bl-2 | Cv-1 | Gbl-1 | Gbl-2 | |
Rb (ppm) | 76 | 55 | 164·1 | 174·5 | 181·9 | 146·7 | 172·9 | 185 | 132 | 138·2 | 171 |
Sr (ppm) | 555·8 | 606·1 | 486·9 | 437·6 | 410·3 | 417·7 | 398·5 | 439·1 | 404·6 | 547·5 | 221·3 |
87Rb/86Sr | 0·3955 | 0·2627 | 0·9767 | 1·1544 | 1·2838 | 1·0167 | 1·2564 | 1·2189 | 0·9438 | 0·7305 | 2·2389 |
87Sr/86Sr | 0·70700(3) | 0·70638(3) | 0·71258(4) | 0·71367(3) | 0·71434(4) | 0·71209(3) | 0·71373(4) | 0·71434(3) | 0·71362(4) | 0·71114(4) | 0·71863(4) |
87Sr/86Sr350 | 0·70503 | 0·70507 | 0·70771 | 0·70792 | 0·70794 | 0·70703 | 0·70747 | 0·70827 | 0·70891 | 0·70750 | 0·70747 |
Sm (ppm) | 4·57 | 6·66 | 5·91 | 5·36 | 5·04 | 6·23 | — | 6·85 | 10·83 | 6·39 | 6·09 |
Nd (ppm) | 24·2 | 33·9 | 31·7 | 28·9 | 26·7 | 33·4 | — | 43·8 | 50·1 | 31·7 | 26·9 |
147Sm/144Nd | 0·1188 | 0·1189 | 0·1128 | 0·1121 | 0·1141 | 0·1127 | — | 0·0946 | 0·1307 | 0·1217 | 0·1366 |
143Nd/144Nd | 0·512476(6) | 0·512479(7) | 0·512210(7) | 0·512186(5) | 0·512187(7) | 0·512267(7) | — | 0·512101(7) | 0·512225(6) | 0·512316 | 0·512334(7) |
143Nd/144Nd350 | 0·512204 | 0·512207 | 0·511952 | 0·511929 | 0·511926 | 0·512009 | — | 0·511884 | 0·511925 | 0·512037 | 0·512021 |
εNd350 | 0·3 | 0·4 | −4·6 | −5·0 | −5·1 | −3·5 | — | −5·9 | −5·1 | −2·9 | −3·2 |
Čertovo břemeno suite | Říčany suite | ||||||||||
Intrusion: | Sedlčany | minettes | Říčany | ||||||||
Se-1 | Se-5 | Se-9 | Mi-2 | Mi-1 | Ri-1 | Ri-2 | Ri-4 | Ri-5 | Ri-6 | Ri-10 | |
Rb (ppm) | 310·9 | 314·4 | 308·1 | 350 | 421·8 | 310·7 | 326·9 | 319·2 | 310·4 | 317·3 | 322·9 |
Sr (ppm) | 313·9 | 339 | 307·8 | 333·7 | 354·1 | 374·1 | 360·2 | 377·7 | 399·5 | 386·6 | 322·4 |
87Rb/86Sr | 2·8703 | 2·6879 | 2·9016 | 3·0408 | 3·4540 | 2·4058 | 2·6299 | 2·4483 | 2·2510 | 2·3776 | 2·9034 |
87Sr/86Sr | 0·72615(3) | 0·72543(3) | 0·72620(3) | 0·72700(4) | 0·72907(4) | 0·72154(3) | 0·72267(3) | 0·72216(4) | 0·72134(4) | 0·72186(3) | 0·72431(3) |
87Sr/86Sr350 | 0·71185 | 0·71204 | 0·71174 | 0·71185 | 0·71187 | 0·70955 | 0·70956 | 0·70996 | 0·71013 | 0·71001 | 0·70984 |
Sm (ppm) | 8·26 | 7·88 | 8·17 | 16·25 | 12·60 | 4·06 | 4·98 | 4·59 | 3·83 | 4·56 | 4·40 |
Nd (ppm) | 40·0 | 40·2 | 40·2 | 75·9 | 61·7 | 24·1 | 29·0 | 27·9 | 23·6 | 28·1 | 26·5 |
147Sm/144Nd | 0·1253 | 0·1186 | 0·1228 | 0·1293 | 0·1235 | 0·1020 | 0·1005 | 0·0995 | 0·0980 | 0·0980 | 0·1005 |
143Nd/144Nd | 0·512114(7) | 0·512103(8) | 0·512080(10) | 0·512140(7) | 0·512113(7) | 0·512053(6) | 0·512035(6) | 0·512062(11) | 0·512074(14) | 0·512068(7) | 0·512075(9) |
143Nd/144Nd350 | 0·511827 | 0·511831 | 0·511799 | 0·511844 | 0·51183 | 0·511819 | 0·511805 | 0·511834 | 0·511849 | 0·511843 | 0·511845 |
εNd350 | −7·0 | −7·0 | −7·6 | −6·7 | −7·0 | −7·2 | −7·5 | −6·9 | −6·6 | −6·7 | −6·7 |
Čertovo břemeno suite | Říčany suite | ||||||||||
Intrusion: | Sedlčany | minettes | Říčany | ||||||||
Se-1 | Se-5 | Se-9 | Mi-2 | Mi-1 | Ri-1 | Ri-2 | Ri-4 | Ri-5 | Ri-6 | Ri-10 | |
Rb (ppm) | 310·9 | 314·4 | 308·1 | 350 | 421·8 | 310·7 | 326·9 | 319·2 | 310·4 | 317·3 | 322·9 |
Sr (ppm) | 313·9 | 339 | 307·8 | 333·7 | 354·1 | 374·1 | 360·2 | 377·7 | 399·5 | 386·6 | 322·4 |
87Rb/86Sr | 2·8703 | 2·6879 | 2·9016 | 3·0408 | 3·4540 | 2·4058 | 2·6299 | 2·4483 | 2·2510 | 2·3776 | 2·9034 |
87Sr/86Sr | 0·72615(3) | 0·72543(3) | 0·72620(3) | 0·72700(4) | 0·72907(4) | 0·72154(3) | 0·72267(3) | 0·72216(4) | 0·72134(4) | 0·72186(3) | 0·72431(3) |
87Sr/86Sr350 | 0·71185 | 0·71204 | 0·71174 | 0·71185 | 0·71187 | 0·70955 | 0·70956 | 0·70996 | 0·71013 | 0·71001 | 0·70984 |
Sm (ppm) | 8·26 | 7·88 | 8·17 | 16·25 | 12·60 | 4·06 | 4·98 | 4·59 | 3·83 | 4·56 | 4·40 |
Nd (ppm) | 40·0 | 40·2 | 40·2 | 75·9 | 61·7 | 24·1 | 29·0 | 27·9 | 23·6 | 28·1 | 26·5 |
147Sm/144Nd | 0·1253 | 0·1186 | 0·1228 | 0·1293 | 0·1235 | 0·1020 | 0·1005 | 0·0995 | 0·0980 | 0·0980 | 0·1005 |
143Nd/144Nd | 0·512114(7) | 0·512103(8) | 0·512080(10) | 0·512140(7) | 0·512113(7) | 0·512053(6) | 0·512035(6) | 0·512062(11) | 0·512074(14) | 0·512068(7) | 0·512075(9) |
143Nd/144Nd350 | 0·511827 | 0·511831 | 0·511799 | 0·511844 | 0·51183 | 0·511819 | 0·511805 | 0·511834 | 0·511849 | 0·511843 | 0·511845 |
εNd350 | −7·0 | −7·0 | −7·6 | −6·7 | −7·0 | −7·2 | −7·5 | −6·9 | −6·6 | −6·7 | −6·7 |
Analytical details have been given by Janoušek et al. (1995); sample descriptions and locations are given in Table 1 and by Janoušek et al. (1995); errors in parentheses are 2 SE.
GEOCHEMICAL MODELLING
The causes of the geochemical variation within each suite were investigated using major- and trace-element modelling. In the case of the fractional crystallization, major-element modelling was based on the general least-squares mixing equation of Bryan et al. (1969) and was performed using the IgPet package. Those oxides that were not determined or that had very low concentrations in all the studied minerals and rocks (MnO and P2O5) were omitted; total iron content (FeOT) was used instead of the separate FeO and Fe2O3. Typical mineral analyses for each particular intrusion were used (Janoušek, 1994); the choice of whole-rock end-members was based on Harker plots and the R1–R2 plot (Fig. 7: De la Roche et al, 1980; Batchelor & Bowden, 1985). The quality of the model was assessed by the sum of squares of the residuals (R2), with R2 = 0 for the ideal fit; R2 < 1 was considered to be acceptable. This approach was repeated for several parent–daughter combinations to check the robustness of the modelling; the ranges of obtained solutions are given below and representative examples are given in Table 3. The major-element, Rb–Sr–Ba and, if applicable, REE data were then modelled using the fractionation schemes derived from the major elements (see Table 4 for distribution coefficients).
plg2 An54* | bi3 | amph7 | Sa-4† | Sa-11† | Difference | Solution‡ | Cumulate§ | ||
Sa-3 | Sa-3 | Sa-3 | recalc 100% | recalc 100% | (obs – calc) | Sa-4 | 1·000 | % | |
Sázava intrusion | |||||||||
SiO2 | 53·41 | 35·32 | 45·35 | 51·61 | 65·02 | 0·00 | plg | −0·345 | 42·8 |
TiO2 | 0·00 | 2·11 | 1·39 | 0·84 | 0·54 | 0·06 | bi | −0·043 | 5·3 |
Al2O3 | 29·48 | 15·31 | 9·47 | 17·88 | 15·95 | −0·06 | amph | −0·418 | 51·9 |
FeOT | 0·09 | 23·56 | 18·57 | 9·79 | 5·73 | −0·24 | Sa-11 | 0·189 | R2 = 0·314 |
MgO | 0·00 | 9·05 | 9·82 | 5·27 | 2·17 | 0·30 | |||
CaO | 11·27 | 0·01 | 11·92 | 10·09 | 5·35 | 0·13 | |||
Na2O | 5·05 | 0·10 | 1·08 | 2·88 | 3·45 | 0·01 | |||
K2O | 0·12 | 9·81 | 1·02 | 1·63 | 1·79 | 0·38 |
plg2 An54* | bi3 | amph7 | Sa-4† | Sa-11† | Difference | Solution‡ | Cumulate§ | ||
Sa-3 | Sa-3 | Sa-3 | recalc 100% | recalc 100% | (obs – calc) | Sa-4 | 1·000 | % | |
Sázava intrusion | |||||||||
SiO2 | 53·41 | 35·32 | 45·35 | 51·61 | 65·02 | 0·00 | plg | −0·345 | 42·8 |
TiO2 | 0·00 | 2·11 | 1·39 | 0·84 | 0·54 | 0·06 | bi | −0·043 | 5·3 |
Al2O3 | 29·48 | 15·31 | 9·47 | 17·88 | 15·95 | −0·06 | amph | −0·418 | 51·9 |
FeOT | 0·09 | 23·56 | 18·57 | 9·79 | 5·73 | −0·24 | Sa-11 | 0·189 | R2 = 0·314 |
MgO | 0·00 | 9·05 | 9·82 | 5·27 | 2·17 | 0·30 | |||
CaO | 11·27 | 0·01 | 11·92 | 10·09 | 5·35 | 0·13 | |||
Na2O | 5·05 | 0·10 | 1·08 | 2·88 | 3·45 | 0·01 | |||
K2O | 0·12 | 9·81 | 1·02 | 1·63 | 1·79 | 0·38 |
plg10 An50 | KF1 | bi4 | amph5 | Koz-9 | Koz-12 | Difference | Solution | Cumulate | ||
Koz-2 | Koz-4 | Koz4 | Koz4 | recalc 100% | recalc 100% | (obs – calc) | Koz-9 | 1·000 | % | |
Kozárovice intrusion | ||||||||||
SiO2 | 54·13 | 63·01 | 35·60 | 45·95 | 59·18 | 66·35 | −0·02 | plg | −0·139 | 32·4 |
TiO2 | 0·04 | 0·00 | 3·80 | 1·04 | 0·81 | 0·59 | 0·05 | KF | −0·053 | 12·3 |
Al2O3 | 29·96 | 19·35 | 14·66 | 7·55 | 16·22 | 15·40 | 0·03 | bi | −0·056 | 13·0 |
FeOT | 0·06 | 0·09 | 19·47 | 16·10 | 6·12 | 4·04 | −0·38 | amph | −0·181 | 42·3 |
MgO | 0·00 | 0·00 | 10·02 | 11·29 | 4·82 | 2·463 | 0·71 | Koz-12 | 0·566 | R2 =0·798 |
CaO | 10·49 | 0·04 | 0·03 | 11·79 | 5·53 | 3·53 | −0·15 | |||
Na2O | 5·53 | 1·05 | 0·12 | 1·29 | 3·23 | 3·20 | 0·35 | |||
K2O | 0·11 | 14·93 | 9·39 | 0·86 | 4·09 | 4·46 | 0·03 |
plg10 An50 | KF1 | bi4 | amph5 | Koz-9 | Koz-12 | Difference | Solution | Cumulate | ||
Koz-2 | Koz-4 | Koz4 | Koz4 | recalc 100% | recalc 100% | (obs – calc) | Koz-9 | 1·000 | % | |
Kozárovice intrusion | ||||||||||
SiO2 | 54·13 | 63·01 | 35·60 | 45·95 | 59·18 | 66·35 | −0·02 | plg | −0·139 | 32·4 |
TiO2 | 0·04 | 0·00 | 3·80 | 1·04 | 0·81 | 0·59 | 0·05 | KF | −0·053 | 12·3 |
Al2O3 | 29·96 | 19·35 | 14·66 | 7·55 | 16·22 | 15·40 | 0·03 | bi | −0·056 | 13·0 |
FeOT | 0·06 | 0·09 | 19·47 | 16·10 | 6·12 | 4·04 | −0·38 | amph | −0·181 | 42·3 |
MgO | 0·00 | 0·00 | 10·02 | 11·29 | 4·82 | 2·463 | 0·71 | Koz-12 | 0·566 | R2 =0·798 |
CaO | 10·49 | 0·04 | 0·03 | 11·79 | 5·53 | 3·53 | −0·15 | |||
Na2O | 5·53 | 1·05 | 0·12 | 1·29 | 3·23 | 3·20 | 0·35 | |||
K2O | 0·11 | 14·93 | 9·39 | 0·86 | 4·09 | 4·46 | 0·03 |
amph1 | plg 3An38 | bi1 | Cv-3 | Bl-1 | Difference | Solution | Cumulate | ||
Bl-5 | Bl-7 | Bl-7 | recalc 100% | recalc 100% | (obs – calc) | Cv-3 | 1·000 | % | |
Blatná intrusion | |||||||||
SiO2 | 45·75 | 57·49 | 36·04 | 63·30 | 68·51 | 0·02 | amph | −0·081 | 26·2 |
TiO2 | 1·15 | 0·00 | 3·35 | 0·75 | 0·51 | 0·00 | plg | −0·144 | 46·8 |
Al2O3 | 7·02 | 26·69 | 14·59 | 16·55 | 15·20 | 0·17 | bi | −0·083 | 26·9 |
FeOT | 16·41 | 0·02 | 18·90 | 5·02 | 3·23 | −0·29 | Bl-1 | 0·699 | R2 = 0·813 |
MgO | 11·74 | 0·00 | 11·28 | 3·66 | 1·86 | 0·38 | |||
CaO | 11·89 | 8·04 | 0·03 | 4·07 | 2·82 | −0·07 | |||
Na2O | 1·16 | 7·02 | 0·11 | 3·01 | 3·72 | −0·72 | |||
K2O | 0·78 | 0·16 | 9·61 | 3·64 | 4·16 | −0·20 |
amph1 | plg 3An38 | bi1 | Cv-3 | Bl-1 | Difference | Solution | Cumulate | ||
Bl-5 | Bl-7 | Bl-7 | recalc 100% | recalc 100% | (obs – calc) | Cv-3 | 1·000 | % | |
Blatná intrusion | |||||||||
SiO2 | 45·75 | 57·49 | 36·04 | 63·30 | 68·51 | 0·02 | amph | −0·081 | 26·2 |
TiO2 | 1·15 | 0·00 | 3·35 | 0·75 | 0·51 | 0·00 | plg | −0·144 | 46·8 |
Al2O3 | 7·02 | 26·69 | 14·59 | 16·55 | 15·20 | 0·17 | bi | −0·083 | 26·9 |
FeOT | 16·41 | 0·02 | 18·90 | 5·02 | 3·23 | −0·29 | Bl-1 | 0·699 | R2 = 0·813 |
MgO | 11·74 | 0·00 | 11·28 | 3·66 | 1·86 | 0·38 | |||
CaO | 11·89 | 8·04 | 0·03 | 4·07 | 2·82 | −0·07 | |||
Na2O | 1·16 | 7·02 | 0·11 | 3·01 | 3·72 | −0·72 | |||
K2O | 0·78 | 0·16 | 9·61 | 3·64 | 4·16 | −0·20 |
bi1 | plg3An42 | KF1 | amph4 | Se-6 | Se-12 | Difference | Solution | Cumulate | ||
Se-6 | Se-5 | Se-5 | Se-9 | recalc 100% | recalc 100% | (obs – calc) | Se-6 | 1·000 | % | |
Sedlčany intrusion | ||||||||||
SiO2 | 36·85 | 56·61 | 62·99 | 50·82 | 67·95 | 69·88 | 0·00 | bi | −0·016 | 11·9 |
TiO2 | 2·95 | 0·02 | 0·02 | 0·36 | 0·57 | 0·54 | −0·05 | KF | −0·057 | 41·8 |
Al2O3 | 14·15 | 26·82 | 18·69 | 4·15 | 14·99 | 14·54 | 0·04 | plg | −0·040 | 29·4 |
FeOT | 16·28 | 0·08 | 0·07 | 13·86 | 2·87 | 2·72 | 0·09 | amph | −0·023 | 16·9 |
MgO | 13·82 | 0·00 | 0·00 | 14·71 | 2·61 | 2·22 | −0·11 | Se-12 | 0·861 | R2 =0·071 |
CaO | 0·00 | 8·63 | 0·05 | 11·22 | 2·39 | 2·08 | 0·02 | |||
Na2O | 0·08 | 6·51 | 0·89 | 0·89 | 2·75 | 2·56 | −0·21 | |||
K2O | 10·03 | 0·22 | 15·35 | 0·37 | 5·80 | 5·42 | −0·05 |
bi1 | plg3An42 | KF1 | amph4 | Se-6 | Se-12 | Difference | Solution | Cumulate | ||
Se-6 | Se-5 | Se-5 | Se-9 | recalc 100% | recalc 100% | (obs – calc) | Se-6 | 1·000 | % | |
Sedlčany intrusion | ||||||||||
SiO2 | 36·85 | 56·61 | 62·99 | 50·82 | 67·95 | 69·88 | 0·00 | bi | −0·016 | 11·9 |
TiO2 | 2·95 | 0·02 | 0·02 | 0·36 | 0·57 | 0·54 | −0·05 | KF | −0·057 | 41·8 |
Al2O3 | 14·15 | 26·82 | 18·69 | 4·15 | 14·99 | 14·54 | 0·04 | plg | −0·040 | 29·4 |
FeOT | 16·28 | 0·08 | 0·07 | 13·86 | 2·87 | 2·72 | 0·09 | amph | −0·023 | 16·9 |
MgO | 13·82 | 0·00 | 0·00 | 14·71 | 2·61 | 2·22 | −0·11 | Se-12 | 0·861 | R2 =0·071 |
CaO | 0·00 | 8·63 | 0·05 | 11·22 | 2·39 | 2·08 | 0·02 | |||
Na2O | 0·08 | 6·51 | 0·89 | 0·89 | 2·75 | 2·56 | −0·21 | |||
K2O | 10·03 | 0·22 | 15·35 | 0·37 | 5·80 | 5·42 | −0·05 |
FeOT total iron as FeO.
*Mineral analyses (Janoušek, 1994).
†Original whole-rock analyses of presumed parent and daughter recalculated to 100%.
‡Proportion of particular minerals removed relative to the parent (=1); (1 − total) × 100 corresponds to degree of fractionation (here 81·1%).
§Percentage of particular minerals in the cumulate.
plg2 An54* | bi3 | amph7 | Sa-4† | Sa-11† | Difference | Solution‡ | Cumulate§ | ||
Sa-3 | Sa-3 | Sa-3 | recalc 100% | recalc 100% | (obs – calc) | Sa-4 | 1·000 | % | |
Sázava intrusion | |||||||||
SiO2 | 53·41 | 35·32 | 45·35 | 51·61 | 65·02 | 0·00 | plg | −0·345 | 42·8 |
TiO2 | 0·00 | 2·11 | 1·39 | 0·84 | 0·54 | 0·06 | bi | −0·043 | 5·3 |
Al2O3 | 29·48 | 15·31 | 9·47 | 17·88 | 15·95 | −0·06 | amph | −0·418 | 51·9 |
FeOT | 0·09 | 23·56 | 18·57 | 9·79 | 5·73 | −0·24 | Sa-11 | 0·189 | R2 = 0·314 |
MgO | 0·00 | 9·05 | 9·82 | 5·27 | 2·17 | 0·30 | |||
CaO | 11·27 | 0·01 | 11·92 | 10·09 | 5·35 | 0·13 | |||
Na2O | 5·05 | 0·10 | 1·08 | 2·88 | 3·45 | 0·01 | |||
K2O | 0·12 | 9·81 | 1·02 | 1·63 | 1·79 | 0·38 |
plg2 An54* | bi3 | amph7 | Sa-4† | Sa-11† | Difference | Solution‡ | Cumulate§ | ||
Sa-3 | Sa-3 | Sa-3 | recalc 100% | recalc 100% | (obs – calc) | Sa-4 | 1·000 | % | |
Sázava intrusion | |||||||||
SiO2 | 53·41 | 35·32 | 45·35 | 51·61 | 65·02 | 0·00 | plg | −0·345 | 42·8 |
TiO2 | 0·00 | 2·11 | 1·39 | 0·84 | 0·54 | 0·06 | bi | −0·043 | 5·3 |
Al2O3 | 29·48 | 15·31 | 9·47 | 17·88 | 15·95 | −0·06 | amph | −0·418 | 51·9 |
FeOT | 0·09 | 23·56 | 18·57 | 9·79 | 5·73 | −0·24 | Sa-11 | 0·189 | R2 = 0·314 |
MgO | 0·00 | 9·05 | 9·82 | 5·27 | 2·17 | 0·30 | |||
CaO | 11·27 | 0·01 | 11·92 | 10·09 | 5·35 | 0·13 | |||
Na2O | 5·05 | 0·10 | 1·08 | 2·88 | 3·45 | 0·01 | |||
K2O | 0·12 | 9·81 | 1·02 | 1·63 | 1·79 | 0·38 |
plg10 An50 | KF1 | bi4 | amph5 | Koz-9 | Koz-12 | Difference | Solution | Cumulate | ||
Koz-2 | Koz-4 | Koz4 | Koz4 | recalc 100% | recalc 100% | (obs – calc) | Koz-9 | 1·000 | % | |
Kozárovice intrusion | ||||||||||
SiO2 | 54·13 | 63·01 | 35·60 | 45·95 | 59·18 | 66·35 | −0·02 | plg | −0·139 | 32·4 |
TiO2 | 0·04 | 0·00 | 3·80 | 1·04 | 0·81 | 0·59 | 0·05 | KF | −0·053 | 12·3 |
Al2O3 | 29·96 | 19·35 | 14·66 | 7·55 | 16·22 | 15·40 | 0·03 | bi | −0·056 | 13·0 |
FeOT | 0·06 | 0·09 | 19·47 | 16·10 | 6·12 | 4·04 | −0·38 | amph | −0·181 | 42·3 |
MgO | 0·00 | 0·00 | 10·02 | 11·29 | 4·82 | 2·463 | 0·71 | Koz-12 | 0·566 | R2 =0·798 |
CaO | 10·49 | 0·04 | 0·03 | 11·79 | 5·53 | 3·53 | −0·15 | |||
Na2O | 5·53 | 1·05 | 0·12 | 1·29 | 3·23 | 3·20 | 0·35 | |||
K2O | 0·11 | 14·93 | 9·39 | 0·86 | 4·09 | 4·46 | 0·03 |
plg10 An50 | KF1 | bi4 | amph5 | Koz-9 | Koz-12 | Difference | Solution | Cumulate | ||
Koz-2 | Koz-4 | Koz4 | Koz4 | recalc 100% | recalc 100% | (obs – calc) | Koz-9 | 1·000 | % | |
Kozárovice intrusion | ||||||||||
SiO2 | 54·13 | 63·01 | 35·60 | 45·95 | 59·18 | 66·35 | −0·02 | plg | −0·139 | 32·4 |
TiO2 | 0·04 | 0·00 | 3·80 | 1·04 | 0·81 | 0·59 | 0·05 | KF | −0·053 | 12·3 |
Al2O3 | 29·96 | 19·35 | 14·66 | 7·55 | 16·22 | 15·40 | 0·03 | bi | −0·056 | 13·0 |
FeOT | 0·06 | 0·09 | 19·47 | 16·10 | 6·12 | 4·04 | −0·38 | amph | −0·181 | 42·3 |
MgO | 0·00 | 0·00 | 10·02 | 11·29 | 4·82 | 2·463 | 0·71 | Koz-12 | 0·566 | R2 =0·798 |
CaO | 10·49 | 0·04 | 0·03 | 11·79 | 5·53 | 3·53 | −0·15 | |||
Na2O | 5·53 | 1·05 | 0·12 | 1·29 | 3·23 | 3·20 | 0·35 | |||
K2O | 0·11 | 14·93 | 9·39 | 0·86 | 4·09 | 4·46 | 0·03 |
amph1 | plg 3An38 | bi1 | Cv-3 | Bl-1 | Difference | Solution | Cumulate | ||
Bl-5 | Bl-7 | Bl-7 | recalc 100% | recalc 100% | (obs – calc) | Cv-3 | 1·000 | % | |
Blatná intrusion | |||||||||
SiO2 | 45·75 | 57·49 | 36·04 | 63·30 | 68·51 | 0·02 | amph | −0·081 | 26·2 |
TiO2 | 1·15 | 0·00 | 3·35 | 0·75 | 0·51 | 0·00 | plg | −0·144 | 46·8 |
Al2O3 | 7·02 | 26·69 | 14·59 | 16·55 | 15·20 | 0·17 | bi | −0·083 | 26·9 |
FeOT | 16·41 | 0·02 | 18·90 | 5·02 | 3·23 | −0·29 | Bl-1 | 0·699 | R2 = 0·813 |
MgO | 11·74 | 0·00 | 11·28 | 3·66 | 1·86 | 0·38 | |||
CaO | 11·89 | 8·04 | 0·03 | 4·07 | 2·82 | −0·07 | |||
Na2O | 1·16 | 7·02 | 0·11 | 3·01 | 3·72 | −0·72 | |||
K2O | 0·78 | 0·16 | 9·61 | 3·64 | 4·16 | −0·20 |
amph1 | plg 3An38 | bi1 | Cv-3 | Bl-1 | Difference | Solution | Cumulate | ||
Bl-5 | Bl-7 | Bl-7 | recalc 100% | recalc 100% | (obs – calc) | Cv-3 | 1·000 | % | |
Blatná intrusion | |||||||||
SiO2 | 45·75 | 57·49 | 36·04 | 63·30 | 68·51 | 0·02 | amph | −0·081 | 26·2 |
TiO2 | 1·15 | 0·00 | 3·35 | 0·75 | 0·51 | 0·00 | plg | −0·144 | 46·8 |
Al2O3 | 7·02 | 26·69 | 14·59 | 16·55 | 15·20 | 0·17 | bi | −0·083 | 26·9 |
FeOT | 16·41 | 0·02 | 18·90 | 5·02 | 3·23 | −0·29 | Bl-1 | 0·699 | R2 = 0·813 |
MgO | 11·74 | 0·00 | 11·28 | 3·66 | 1·86 | 0·38 | |||
CaO | 11·89 | 8·04 | 0·03 | 4·07 | 2·82 | −0·07 | |||
Na2O | 1·16 | 7·02 | 0·11 | 3·01 | 3·72 | −0·72 | |||
K2O | 0·78 | 0·16 | 9·61 | 3·64 | 4·16 | −0·20 |
bi1 | plg3An42 | KF1 | amph4 | Se-6 | Se-12 | Difference | Solution | Cumulate | ||
Se-6 | Se-5 | Se-5 | Se-9 | recalc 100% | recalc 100% | (obs – calc) | Se-6 | 1·000 | % | |
Sedlčany intrusion | ||||||||||
SiO2 | 36·85 | 56·61 | 62·99 | 50·82 | 67·95 | 69·88 | 0·00 | bi | −0·016 | 11·9 |
TiO2 | 2·95 | 0·02 | 0·02 | 0·36 | 0·57 | 0·54 | −0·05 | KF | −0·057 | 41·8 |
Al2O3 | 14·15 | 26·82 | 18·69 | 4·15 | 14·99 | 14·54 | 0·04 | plg | −0·040 | 29·4 |
FeOT | 16·28 | 0·08 | 0·07 | 13·86 | 2·87 | 2·72 | 0·09 | amph | −0·023 | 16·9 |
MgO | 13·82 | 0·00 | 0·00 | 14·71 | 2·61 | 2·22 | −0·11 | Se-12 | 0·861 | R2 =0·071 |
CaO | 0·00 | 8·63 | 0·05 | 11·22 | 2·39 | 2·08 | 0·02 | |||
Na2O | 0·08 | 6·51 | 0·89 | 0·89 | 2·75 | 2·56 | −0·21 | |||
K2O | 10·03 | 0·22 | 15·35 | 0·37 | 5·80 | 5·42 | −0·05 |
bi1 | plg3An42 | KF1 | amph4 | Se-6 | Se-12 | Difference | Solution | Cumulate | ||
Se-6 | Se-5 | Se-5 | Se-9 | recalc 100% | recalc 100% | (obs – calc) | Se-6 | 1·000 | % | |
Sedlčany intrusion | ||||||||||
SiO2 | 36·85 | 56·61 | 62·99 | 50·82 | 67·95 | 69·88 | 0·00 | bi | −0·016 | 11·9 |
TiO2 | 2·95 | 0·02 | 0·02 | 0·36 | 0·57 | 0·54 | −0·05 | KF | −0·057 | 41·8 |
Al2O3 | 14·15 | 26·82 | 18·69 | 4·15 | 14·99 | 14·54 | 0·04 | plg | −0·040 | 29·4 |
FeOT | 16·28 | 0·08 | 0·07 | 13·86 | 2·87 | 2·72 | 0·09 | amph | −0·023 | 16·9 |
MgO | 13·82 | 0·00 | 0·00 | 14·71 | 2·61 | 2·22 | −0·11 | Se-12 | 0·861 | R2 =0·071 |
CaO | 0·00 | 8·63 | 0·05 | 11·22 | 2·39 | 2·08 | 0·02 | |||
Na2O | 0·08 | 6·51 | 0·89 | 0·89 | 2·75 | 2·56 | −0·21 | |||
K2O | 10·03 | 0·22 | 15·35 | 0·37 | 5·80 | 5·42 | −0·05 |
FeOT total iron as FeO.
*Mineral analyses (Janoušek, 1994).
†Original whole-rock analyses of presumed parent and daughter recalculated to 100%.
‡Proportion of particular minerals removed relative to the parent (=1); (1 − total) × 100 corresponds to degree of fractionation (here 81·1%).
§Percentage of particular minerals in the cumulate.
Mineral | La | Ce | Nd | Sm | Eu | Gd | Tb | Yb | Lu | Ref. | Y | Ref. | Rb | Sr | Ba | Ref. |
amphibole | 0·85 | 1·2 | 3·2 | 5·4 | 3·6 | 10 (1) | 3 | 6·2 | 4·5 | (2) | 6 | (3) | 0·014 | 0·22 | 0·044 | (4) |
plagioclase | 0·32 | 0·24 | 0·19 | 0·13 | 2·00 | 0·16 | 0·15 | 0·08 | 0·06 | (2) | 0·1 | (3) | 0·041 | 4·4 | 0·31 | (4) |
biotite | 0·32 | 0·04 | 0·04 | 0·06 | 0·15 | 0·44 | 0·39 | 0·67 | 0·74 | (2) | 0·03 | (3) | 3·26 | 0·12 | 6·36 | (4) |
K-feldspar | 0·072 | 0·046 | 0·038 | 0·025 | 2·6 | 0·011 | 0·033 | 0·02 | 0·03 | (3) | 0·659 | 3·87 | 6·12 | (4) | ||
allanite | 1331 | 1279 | 874 | 438 | 107 | 214 | 204 | 22 | 22 | (5) | ||||||
titanite | 60 | 90 | 103 | 340 | 157 | 383 | 326 | 231 | 176 | (5) | ||||||
zircon | 3·3 | 2·4 | 2·2 | 3·7 | 3·4 | 13·9 | 26·3 | 225 | 300 | (5) | ||||||
apatite | 46·1 | 41·6 | 55·8 | 65 | 27·3 | 79 | 60 | 60 | 60 | (5) |
Mineral | La | Ce | Nd | Sm | Eu | Gd | Tb | Yb | Lu | Ref. | Y | Ref. | Rb | Sr | Ba | Ref. |
amphibole | 0·85 | 1·2 | 3·2 | 5·4 | 3·6 | 10 (1) | 3 | 6·2 | 4·5 | (2) | 6 | (3) | 0·014 | 0·22 | 0·044 | (4) |
plagioclase | 0·32 | 0·24 | 0·19 | 0·13 | 2·00 | 0·16 | 0·15 | 0·08 | 0·06 | (2) | 0·1 | (3) | 0·041 | 4·4 | 0·31 | (4) |
biotite | 0·32 | 0·04 | 0·04 | 0·06 | 0·15 | 0·44 | 0·39 | 0·67 | 0·74 | (2) | 0·03 | (3) | 3·26 | 0·12 | 6·36 | (4) |
K-feldspar | 0·072 | 0·046 | 0·038 | 0·025 | 2·6 | 0·011 | 0·033 | 0·02 | 0·03 | (3) | 0·659 | 3·87 | 6·12 | (4) | ||
allanite | 1331 | 1279 | 874 | 438 | 107 | 214 | 204 | 22 | 22 | (5) | ||||||
titanite | 60 | 90 | 103 | 340 | 157 | 383 | 326 | 231 | 176 | (5) | ||||||
zircon | 3·3 | 2·4 | 2·2 | 3·7 | 3·4 | 13·9 | 26·3 | 225 | 300 | (5) | ||||||
apatite | 46·1 | 41·6 | 55·8 | 65 | 27·3 | 79 | 60 | 60 | 60 | (5) |
References: (1) Martin (1987); (2) Henderson (1982); (3) Rollinson (1993) and references therein; (4) Hanson (1978); (5) Sawka (1988).
Mineral | La | Ce | Nd | Sm | Eu | Gd | Tb | Yb | Lu | Ref. | Y | Ref. | Rb | Sr | Ba | Ref. |
amphibole | 0·85 | 1·2 | 3·2 | 5·4 | 3·6 | 10 (1) | 3 | 6·2 | 4·5 | (2) | 6 | (3) | 0·014 | 0·22 | 0·044 | (4) |
plagioclase | 0·32 | 0·24 | 0·19 | 0·13 | 2·00 | 0·16 | 0·15 | 0·08 | 0·06 | (2) | 0·1 | (3) | 0·041 | 4·4 | 0·31 | (4) |
biotite | 0·32 | 0·04 | 0·04 | 0·06 | 0·15 | 0·44 | 0·39 | 0·67 | 0·74 | (2) | 0·03 | (3) | 3·26 | 0·12 | 6·36 | (4) |
K-feldspar | 0·072 | 0·046 | 0·038 | 0·025 | 2·6 | 0·011 | 0·033 | 0·02 | 0·03 | (3) | 0·659 | 3·87 | 6·12 | (4) | ||
allanite | 1331 | 1279 | 874 | 438 | 107 | 214 | 204 | 22 | 22 | (5) | ||||||
titanite | 60 | 90 | 103 | 340 | 157 | 383 | 326 | 231 | 176 | (5) | ||||||
zircon | 3·3 | 2·4 | 2·2 | 3·7 | 3·4 | 13·9 | 26·3 | 225 | 300 | (5) | ||||||
apatite | 46·1 | 41·6 | 55·8 | 65 | 27·3 | 79 | 60 | 60 | 60 | (5) |
Mineral | La | Ce | Nd | Sm | Eu | Gd | Tb | Yb | Lu | Ref. | Y | Ref. | Rb | Sr | Ba | Ref. |
amphibole | 0·85 | 1·2 | 3·2 | 5·4 | 3·6 | 10 (1) | 3 | 6·2 | 4·5 | (2) | 6 | (3) | 0·014 | 0·22 | 0·044 | (4) |
plagioclase | 0·32 | 0·24 | 0·19 | 0·13 | 2·00 | 0·16 | 0·15 | 0·08 | 0·06 | (2) | 0·1 | (3) | 0·041 | 4·4 | 0·31 | (4) |
biotite | 0·32 | 0·04 | 0·04 | 0·06 | 0·15 | 0·44 | 0·39 | 0·67 | 0·74 | (2) | 0·03 | (3) | 3·26 | 0·12 | 6·36 | (4) |
K-feldspar | 0·072 | 0·046 | 0·038 | 0·025 | 2·6 | 0·011 | 0·033 | 0·02 | 0·03 | (3) | 0·659 | 3·87 | 6·12 | (4) | ||
allanite | 1331 | 1279 | 874 | 438 | 107 | 214 | 204 | 22 | 22 | (5) | ||||||
titanite | 60 | 90 | 103 | 340 | 157 | 383 | 326 | 231 | 176 | (5) | ||||||
zircon | 3·3 | 2·4 | 2·2 | 3·7 | 3·4 | 13·9 | 26·3 | 225 | 300 | (5) | ||||||
apatite | 46·1 | 41·6 | 55·8 | 65 | 27·3 | 79 | 60 | 60 | 60 | (5) |
References: (1) Martin (1987); (2) Henderson (1982); (3) Rollinson (1993) and references therein; (4) Hanson (1978); (5) Sawka (1988).
Whenever a magma-mixing scenario was invoked, it was quantified by a mixing test using major elements (Fourcade & Allègre, 1981). Its principle is that all the oxides of a sample that originated by magma mixing should plot on a straight line in a diagram of ca – cb vs ch – cb (where ca, cb and ch stand for wt % oxide in the acid end-member, basic end-member, and suspected hybrid, respectively) with the slope being equivalent to the proportion of the component a. The results were then tested on the trace-element data by comparison of the calculated and observed contents of the putative hybrids (Castro et al., 1990).
Sázava suite
The geochemical characteristics of the Sázava suite (mainly metaluminous, K2O << Na2O; (87Sr/86Sr)350 ∼ 0·705, εNd350 ∼ 0 for the Sázava tonalite; Fig. 6) correspond to those of a typical I-type granitoid (e.g. Clarke, 1992, and references therein). The Harker plots (Fig. 8) show a negative correlation of SiO2 with CaO, MgO, TiO2 and Y, and a positive correlation with K2O, Rb and Ba. Such trends are consistent with fractionation dominated by amphibole and calcic plagioclase, as also revealed by the R1–R2 plot (Fig. 7). A major role for biotite and K-feldspar fractionation is unlikely in view of their interstitial habit (Janoušek, 1994). Least-squares modelling (e.g. Table 3) shows that the compositional spectrum of the Sázava intrusion can be explained by extensive (up to 82%) fractionation of ∼52% amphibole, 43% plagioclase and 5% biotite. A high degree of fractionation (∼65–75%) can be inferred independently from the concentrations of strongly incompatible elements such as Ba (Fig. 8d).
With the Sázava suite showing the least evolved major- and trace-element geochemistry, a primitive Sr–Nd isotopic signature (close to Bulk Earth), and an abundance of mafic microgranular enclaves (interpreted as hybrids of acidic and basic magmas; e.g. Didier & Barbarin, 1991, p. 23), a significant role for mantle-derived material in its genesis is indicated. On the basis of the Sr–Nd isotope data the suite could have formed by (1) crystallization from (asthenospheric?) mantle-derived melts with an isotopic composition close to Bulk Earth, (2) melting of local metabasic rocks that have a similar Sr–Nd signature, or (3) mixing of melts derived from both sources (Janoušek et al., 1995). Although there exists considerable field, microstructural, mineral and whole-rock geochemical evidence for mixing and mingling between mafic and felsic magmas, at least in the western part of the Sázava intrusion (e.g. in Teletín: Dudek & Fediuk, 1957; Janoušek, 1994; Janoušek et al., 1997a; see Fig. 7), derivation for the whole compositional range of the suite in this manner seems unlikely: the associated basic rocks do not form a continuum with the Sázava samples on the R1–R2 plot (Fig. 7), and do not have low enough SiO2 contents (Janoušek, 1994).
Taking into account the near contemporaneity of both the Sázava and Požáry intrusions (Holub et al., 1997a), the Požáry trondhjemites, characterized by low ∑REE and positive Eu anomalies, could, in theory, have been derived in three ways: (1) by plagioclase accumulation from a Sázava-like parent, (2) by fractional crystallization from a similar melt of a largely amphibole–plagioclase assemblage, or (3) by variable, but low degrees of partial melting of a metabasic source leaving amphibole ± garnet in the residue [to explain the observed low middle REE (MREE) and HREE contents].
Although plagioclase accumulation probably played an important role in the genesis of some of the Požáry samples (e.g. Po-1 in Fig. 8, a rock that shows a cumulate-like texture), a purely cumulative origin from the Sázava magma is ruled out because this would require the Sázava melt to be driven towards less silicic compositions. Moreover, such a model would necessitate early crystallization of a plagioclase–quartz assemblage (as the trondhjemites are more silica rich than their feldspars) without a significant proportion of amphibole. This, together with amphibole being only an accessory phase in the trondhjemite, is not in accord with the evidence of early simultaneous crystallization of plagioclase and amphibole in the Sázava intrusion.
The observed progressive decrease in REE and Y contents suggests a major role for either amphibole or some accessory mineral(s) (e.g. titanite, allanite)—the only phases that have distribution coefficients for these elements generally >1. This is consistent with the evidence for amphibole-dominated fractionation inferred from major elements. By 30–50% fractionation of the assemblage for the Sázava intrusion in Table 3 (calculated by the least-squares method), it is possible to generate HREE patterns similar to the trondhjemite from the least evolved Sázava tonalite (Sa-4), although without the observed LREE depletion. For this reason, involvement of an additional phase that concentrates LREE, such as allanite or titanite (e.g. Martin, 1987; Sawka, 1988; Evans & Hanson, 1993), both of which occur in the Sázava suite, is necessary. Addition of as little as 0·1% allanite improves the fit of the model (Fig. 9). Were titanite involved in the calculations, a much higher proportion would be needed (0·5%), and 1% apatite would have to be added to compensate for depletion in MREE and HREE. Thus the combined amphibole–plagioclase–allanite model is preferred, although some apatite had to fractionate to account for the gradually decreasing P2O5 in the Sázava suite. The origin of strikingly similar REE patterns in trondhjemites from Finland was also explained by fractional crystallization of an amphibole > plagioclase + biotite assemblage from a tonalitic parent (Arth et al., 1978). Drawbacks to this model are (1) the amount of fractionation required by the REE is significantly less than that inferred from the modelling of the Sázava intrusion using major and other trace elements and (2) it fails to reproduce accurately the magnitude of the positive Eu anomaly observed for the trondhjemites. Such discrepancies could be caused by uncertainties in the KD values for the REE (which, for Eu, is also strongly dependent on the oxygen fugacity), as well as additional processes, such as interaction with basic melts.
Although the slightly peraluminous nature of the trondhjemite can be accounted for by the fractional crystallization model, as peraluminous granitoids can be produced by extensive fractionation of a metaluminous mineral (such as amphibole) from metaluminous melts, the composition of the trondhjemite is also compatible with a genesis through partial melting of amphibolite with reactions such as amphibole → clinopyroxene + olivine + melt or garnet → clinopyroxene + melt (Miller, 1985). The partial melting of garnet amphibolite or eclogite is capable of generating trondhjemites with low ∑REE, high LREE/HREE and pronounced positive Eu anomalies due to the presence in the residue of amphibole and/or garnet (e.g. Cullers & Graf, 1984). The REE patterns observed in the Požáry trondhjemite resemble those modelled as melts of basaltic parents leaving an amphibolite residue (Hanson, 1980), although at somewhat higher ∑REE.
Apart from direct fractionation from mantle-derived basic rocks, trondhjemites and tonalites can be produced by increasing degrees of partial melting of the same metabasic parent (amphibolite, garnet amphibolite or eclogite; e.g. Rapp et al., 1991). The occurrence of the Sázava suite in the proximity of metabasic roof pendants may support an origin by melting of similar material were these rocks to occur at depth. Hence it is worth considering whether such a link could exist between the Požáry trondhjemite and the Sázava tonalite. For a presumed (garnet–) amphibole residue, Ba, as an incompatible element, would be strongly partitioned into the melt and its concentration therein would sharply decrease with increasing degree of melting. On the other hand, the concentration of compatible elements (Cr, Ni, Co, HREE and Y) in the melt should be buffered at a relatively constant level regardless of the degree of melting. Although there is a sharp decrease in Ba with decreasing SiO2, the concentrations of the above compatible elements increase in the same direction (see examples in Figs 8–10). Hence the partial melting model would also require different parents for both intrusions. Moreover, in the roof pendants of the CBP, metabasites are associated with metasedimentary material, which would be likely to melt first and so strongly influence the Sr–Nd isotopic signature.
In summary, partial melting of metabasites, partial melting of a mantle source with an isotopic signature close to Bulk Earth, or mixing of magmas derived from both sources gave rise to the most primitive rocks of the Sázava intrusion with subsequent extensive fractional crystallization of mainly amphibole and plagioclase producing the intra-suite variation. Either high degrees of fractionation of the Sázava magma or small degrees of melting of a metabasic source could account for the generation of the Požáry trondhjemites.
Blatná suite
The Blatná suite comprises metaluminous to slightly peraluminous high-K calc-alkaline granodiorites and granites, associated with shoshonitic monzonitic rocks. The two largest masses within the Blatná suite—the Kozárovice and Blatná intrusions—have been investigated.
Harker variation diagrams (Fig. 11) show strong negative correlations between SiO2 and FeO*, MnO, MgO, CaO and TiO2, implying fractionation dominated by ferromagnesian phase(s) and possibly plagioclase. A significant role for biotite and/or K-feldspar is suggested by the negative SiO2–Ba correlation.
Least-squares calculations (Table 3, Kozárovice assemblage) suggest that the whole compositional spectrum of the Kozárovice intrusion could have been derived by up to ∼45% fractional crystallization of 35–42% amphibole, 28–33% plagioclase, 7–13% K-feldspar and 13–22% biotite; this is consistent with the Ba–Sr correlation (Fig. 12). The Kozárovice REE patterns (Fig. 5b) are too uniform for quantitative modelling. However, if the assemblage calculated by the least-squares modelling is considered, the following values of the bulk distribution coefficients (D) are obtained: DLa = 1·42, DCe = 1·18, DEu = 2·48 and DLu= 2·01. For ∼40% fractionation, this results in depletions of 10–20% in the LREE, and 40–50% in the MREE and HREE; the Eu anomaly remains nearly constant. The resulting REE pattern falls within the compositional range observed for the Kozárovice intrusion.
The Kozárovice quartz monzonite (KozD-1) may have originated by magma mixing (mingling) between a monzonitic melt and the surrounding granodiorite. This interpretation is supported by microstructural and field evidence such as net-veining of the quartz monzonite, an abundance of mafic microgranular enclaves, and disequilibrium textures in both putative hybrid rocks and the surrounding granodiorite (Janoušek et al., 1997a). The mixing test of Fourcade & Allègre (1981) also supports this hypothesis (Fig. 13), suggesting that ∼70% of the Kozárovice granodiorite mixed with the monzonite. Small discrepancies in the trace-element composition can be explained either by small-scale fractionation or by lack of information concerning the exact composition of the basic end-member.
The Blatná intrusion is somewhat more evolved than the Kozárovice intrusion (Fig. 11). Least-squares modelling of the intrusion (Table 3, Blatná assemblage) requires up to ∼35% fractionation of mainly plagioclase (47–52%), amphibole (17–28%) and biotite (22–31%). This agrees with the Ba–Sr covariations (Fig. 12).
The fact that the content of REE in the less evolved amphibole-rich rocks is significantly higher than in the biotite facies (Fig. 14) implies fractionation of phases with high KD values for the REE, such as amphibole. On the other hand, the slight decrease in the magnitude of the Eu anomaly (from Eu/Eu* = 0·54–0·67 to 0·70–0·74) is consistent with a roughly balanced influence of feldspar and phases contributing to a positive Eu anomaly in the residual melt (e.g. amphibole, clinopyroxene and apatite). The REE pattern calculated for 20–40% fractionation of the assemblage modelled by major elements and LILE agrees with the available data provided that 0·1% allanite, which is present in these rocks, is introduced into the model to reduce the LREE sufficiently.
Although closed-system fractionation schemes can model successfully the major- and trace-element evolution of the Blatná and Kozárovice intrusions, the linear trends on Harker variation diagrams could also be consistent with a model of magma mixing producing the overall variation within the suite (e.g. Machart, 1992), rather than just on a local scale as discussed above for the Kozárovice quartz monzonite. Furthermore, the variation in initial Sr and Nd isotope ratios (Fig. 6) precludes closed-system behaviour within this suite, and suggests that different sources with distinct isotopic compositions were involved. A simple mixing model between the K-rich monzonites and more evolved members of the Blatná suite can, in theory, account for the observed (87Sr/86Sr)350–εNd350 pattern (Janoušek et al., 1995).
However, on a 1/Nd–εNd350 plot, the Kozárovice and Blatná intrusions form independent, curved trends (Fig. 15a). Binary mixing as well as AFC (DePaolo, 1981), in which DNd (bulk distribution coefficient) and r (rate of assimilation/fractional crystallization) are constant, ought to produce linear trends in this diagram (Albarède, 1995). Consequently, these two processes are unlikely to have produced the trends shown. However, curved trends can be explained by changing either DNd or r in the course of the AFC (Powell, 1984). Both cases are modelled here using the slope of two segments of the 1/Nd–εNdi curve (Powell, 1984). The formulae used are given in the Appendix: for the Kozárovice data, these are the Koz-6–Koz-2 and Koz-4–Koz-5 segments, with slopes S1 = −695·9 and S2 = −24·5, respectively (Fig. 15a). In the following text, subscripts ‘1’ and ‘2’, used to specify r and D, refer to the number of the segment.
(1) Constant D (D1 = D2), variable r (r1 > r2)
Such a decrease in r values could possibly reflect a decrease in the temperature of the assimilant encountered by magma ascending through the crust and/or the fact the magma also cools as it crystallizes (see DePaolo, 1981). It should be stressed that this two-step model represents a simplification, as in reality r is likely to change continuously.
Before any assumptions are made about DNd, r1 and r2, a field of possible contaminants can be outlined on the 1/Nd–εNdi plot using equation (6) (see Appendix). For the Kozárovice intrusion, such contaminants could comprise Moldanubian basic granulites and paragneisses (Fig. 15a). The r1 and r2 values can be determined by assuming a certain contaminant composition and DNd [equations (4) and (5)]. Various prospective contaminants were considered using DNd = 2·3, calculated for the assemblage given in Table 3 for this intrusion with the addition of 0·1% allanite. For example, the calculation for paragneiss JT-28 results in r1 = 2·60 and r2 = 0·19.
Although several other assimilants were considered [e.g. more evolved paragneiss CR-5 (r1 = 1·22, r2 = 0·10) and basic granulite 1059 (r1 = 7·46, r2 = 0·39)], of the various two-stage AFC curves plotted onto the (87Sr/86Sr)350–εNd350 diagram, that with JT-28 as the contaminant corresponded most closely to the observed variation (Fig. 15b). The influence of uncertainties imposed by the initial choice of DNd was tested: for DNd = 2–3 and JT-28 as assimilant, r1 = 2–4, r2 = 0·14–0·29.
Although using JT-28 as a contaminant provides a satisfactory fit of the data, the resultant r1 value is unreasonably high (as even the rate of assimilation of hot country rocks is unlikely to exceed the rate of fractional crystallization of the magma, i.e. r should be always lower than about unity: DePaolo, 1981; Taylor & Sheppard, 1986), and so either this model is not feasible, or the contaminant corresponds to an unsampled lithology.
For the Blatná intrusion, Fig. 15c suggests that a similar process could have been operative, although with an essentially different parental composition and more restricted field of possible contaminants (almost solely paragneisses). Calculations analogous to those of the previous case (first segment Cv-1–Bl-2, second Bl-2–11b, DNd = 1·81; Fig. 15a) produced comparable results; for assimilant JT-28, the calculated r1and r2 values were 2·28 and 0·15, respectively. Again, the r1 value is unreasonably high.
(2) Constant r (r1 = r2), variable DNd (D1 < D2)
As no curved trends are apparent on a plot of 1/Sr–(87Sr/86Sr)350 (not shown), it is assumed that DSr did not change during crystallization. In the following modelling, DSr was calculated for the assemblages given in Table 3 for the Kozárovice and Blatná intrusions. However, the curved trends on the 1/Nd–εNd350 diagram (Fig. 15d) imply that DNd and therefore the fractionating assemblage may have changed during the progressive crystallization.
It is difficult to make a priori assumptions about possible contaminants for this model [see Appendix, equation (12)]. Both D1 and D2 can be determined for a given contaminant composition and r [equations (10) and (11)]. Prospective solutions were tested on the (87Sr/86Sr)350–εNd350 diagram (Fig. 15e). For the Kozárovice data, a good fit was obtained using paragneiss JT-28 as an assimilant and r = 0·5; this resulted in D1= 1·25 and D2= 4·51, values that are reasonable (see discussion above). This model requires 20–25% fractionation (Fig. 15e and f). The distribution coefficients for the REE are largely controlled by accessory phases; for instance, for the assemblage given in Table 3 for the Kozárovice intrusion, DNd can be changed from 1·4 to 4·1 by adding as little as 0·3% allanite. The other assimilants (such as granulite 1059 or paragneiss CR-5) failed to reproduce the observed variation in Fig. 15e completely and/or resulted in too high degrees of fractionation.
For the Blatná intrusion, an identical r = 0·5 value was assumed. For the same contaminant, comparable bulk distribution coefficients were obtained (D1 = 1·18, D2 = 3·66), requiring about 30% AFC (Fig. 15f).
In summary, the geochemical variation shown by the Blatná and Kozárovice intrusions reflects open-system processes, probably AFC with variable DNd and Moldanubian paragneisses as a contaminant. Moreover, interaction with monzonitic magmas associated with the suite played an important role. The fractionating assemblage was probably dominated by amphibole > plagioclase + K-feldspar > biotite (Kozárovice intrusion) and plagioclase > biotite > amphibole >> allanite (Blatná intrusion).
Čertovo břemeno suite
The Čertovo břemeno suite is made up of shoshonitic metaluminous to weakly peraluminous melagranites and melasyenites together with minettes. The suite is characterized by high K2O, P2O5, Rb, Zr, Ba and mg-number, and low CaO and Na2O compared with the Sázava and Blatná suites (e.g. Figs 3 and 4; Table 1).
The granitoids of the Čertovo břemeno suite and associated minettes have the most evolved Sr–Nd isotopic compositions within the CBP (Janoušek et al., 1995, 1997b). For the minettes, modelling of simple two-component mixing rules out crustal contamination by material isotopically similar to that from the adjacent Moldanubian and Teplá–Barrandian units as the main mechanism for producing such evolved Sr–Nd compositions. Instead, these are more likely to mirror isotopic compositions of a mantle source that was strongly enriched in incompatible elements (Janoušek et al., 1995, 1997b; Holub, 1997). The presence of such a reservoir beneath the Moldanubian unit was recently assumed by Becker (1996) and Gerdes et al. (1998). The former worker interpreted garnet pyroxenites from Lower Austria as high-pressure cumulates that crystallized from carbonatite, melilite or lamprophyre magmas. These were shown to be partly contemporaneous with the rocks of the Čertovo břemeno suite, and to have overlapping Sr–Nd isotopic compositions. The origin through melting of a variously enriched lithospheric mantle source was also assumed for Hercynian K-rich rocks elsewhere (Turpin, 1988; Wenzel et al., 1997; Hegner et al., 1998).
Given that the geochemistry of the mafic parts of the Čertovo břemeno suite is similar to that of the minettes, and that the minettes and the more evolved Sedlčany granite have identical Sr–Nd isotopic compositions (Tables 1 and 2), the Sedlčany granite could have originated by closed-system fractional crystallization of a parental, mantle-derived magma corresponding to the mafic members of the suite. The variation in the R1–R2 plot points, in theory, to fractionation of Fe-rich biotite, possibly with a significant contribution from K-feldspar and relatively sodic plagioclase (Janoušek, 1994); the Mg-rich composition of the Sedlčany biotite, however, precludes fractionation controlled solely by this mineral. The negative correlation of SiO2 with Ba and K2O, and, to some extent, Sr (Fig. 16) is compatible with fractionation of mainly K-feldspar and biotite, whereas a similar trend for CaO suggests a role for amphibole, and/or plagioclase.
Major-element modelling (Table 3) suggests that the SiO2-rich Sedlčany samples (e.g. Se-12) could have been produced by up to 15–20% fractional crystallization of 30–40% plagioclase, 30–40% K-feldspar, 10–20% biotite and 10–20% amphibole from the SiO2-poor parts of this intrusion (e.g. Se-6). This model appears to be generally supported by the Ba–Sr plot (Fig. 17); the low degree of fractionation, however, does not allow REE-based modelling.
Some of the variation in the Sedlčany granite could have been caused by assimilation processes that are likely to have been accompanied by fractional crystallization (AFC). In its western part, the granite contains many often partially resorbed xenoliths, especially of carbonates, from the adjacent roof pendants of the Metamorphic Islet Zone. On the other hand, the remarkably uniform Sr–Nd isotopic composition of the granite is not compatible with the operation of extensive assimilation of isotopically different material.
An alternative model has been presented by Holub (1997), who, on the basis of petrography and whole-rock geochemistry, argued that the different members of the suite could have been derived by hybridization of mafic durbachites with leucogranites such as those present within the CBP or the S-type granites such as the Eisgarn intrusion of the Moldanubian Pluton further to the east. Although the similarity in Sr isotopic composition between all these components in the potential mixing process precludes the use of Sr isotopes for assessing the mass balance, it is consistent with such a process (Janoušek et al., 1995; Gerdes et al., 1998).
Taken together, the parental magma of the Sedlčany granite could have been produced either by magma mixing between isotopically similar enriched mantle-derived and leucogranitic components, and/or by fractional crystallization from the Čertovo břemeno parent.
Říčany suite
The Říčany suite comprises peraluminous biotite ± muscovite monzogranites and its petrogenesis has been considered by Janoušek et al. (1997c). In summary, the evolved, high-level Říčany intrusion is rich in K2O and Rb, and poor in CaO, MgO and Na2O, with high Ba/Cs and LREE/HREE, and low K/Rb ratios. The Harker variation diagrams offer little scope for genetic considerations because of the very restricted SiO2 range, but the R1–R2 plot (Fig. 7), together with the observed decrease in Sr and Ba, and increase in Rb, with fractionation are compatible with fractionation controlled by K-feldspar. The intrusion shows cryptic reverse zoning, interpreted as being probably due to rearrangement of a single pulse of magma during intrusion from a vertically graded magma chamber at depth. The whole-rock geochemistry and the Sr–Nd isotopic data are compatible with an origin of the granite by melting of evolved material compositionally similar to the Moldanubian paragneisses or leucocratic granulites.
PETROGENESIS AND GEOTECTONIC SETTING OF THE CENTRAL BOHEMIAN PLUTON
The genesis of granitoids of the CBP has been explained by various models, an overview of which has been given by Holub (1992) and Holub et al. (1997b). Holub and coworkers, like us, reject granitization models (e.g. Palivcová et al., 1989a,1989b; Vlašímský et al., 1992) and conclude that all the intrusions were originally magmas, mobile and capable of inducing thermal metamorphism on, and being contaminated by, their country rocks. However, it is also clear that any single closed-system process could not have been responsible for generation of the CBP as a whole (e.g. Fig. 6). The geochemical data presented here, together with petrographic and isotopic evidence (e.g. Holub, 1992; Janoušek et al., 1995; Holub et al., 1997b) indicate major differences in sources as well as a crucial role for fractional crystallization, AFC and magma mixing–mingling processes in the origin of individual suites. Variously enriched lithospheric mantle played a key role in the petrogenesis of the later suites (Blatná and, in particular, Čertovo břemeno), and the mechanism of mantle enrichment and its geotectonic setting are important aspects to be considered in assessing the development of the CBP.
Role of subduction in the genesis of the CBP
In geotectonic terms, the shift towards K-rich calc-alkaline and shoshonitic granitoid magmatism with time in the CBP may be compatible with a transition from a magmatic-arc to a post-collisional setting (e.g. Holub, 1992). Although the various major- and trace-element based discrimination diagrams do not give unequivocal indications of the tectonic setting of the individual suites (Janoušek, 1994; Holub et al., 1997b), the geochemical character of the Sázava suite may point to an origin in a continental arc environment, as suggested especially by its calc-alkaline nature and a pronounced Nb–Ta trough on ocean ridge granite (ORG) normalized multi-element diagrams (Fig. 4).
The operation of subduction in this part of the Bohemian Massif in mid–late Devonian times (∼370 Ma) has been inferred from the geochemistry of orthogneisses occurring as roof pendants of the CBP (Košler, 1993). The direct proof of early Hercynian (older than 360 Ma: 40Ar/39Ar phengite) subduction-related HP–LT metamorphism in the Bohemian Massif comes from studies of Na amphibole-bearing metabasites, occurring to the NE, in the southeastern Krkonoše Mts (Maluski & Patočka, 1997). Occurrences of similar rocks near the margins of the Saxothuringian zone in the Bohemian Massif may trace a dismembered early Hercynian suture zone (Patočka & Novák, 1997). Petrologically and geochemically analogous, roughly coeval granitoid suites, which occur in the Limousin Tonalite Belt (French Massif Central), the Odenwald, the northern Black Forest, as well as in the Alpine basement, could have been also genetically related to early Hercynian subduction (Shaw et al., (1993); Finger et al., 1997).
Were subduction operative in the area of the CBP early in the development of the Hercynian belt, the mantle wedge above the subduction zone would have been fluxed by LILE-enriched and HFSE-depleted fluids. Tapped at a slightly later stage, this might have promoted melting and the generation of basic calc-alkaline magmas that could have fractionated, and/or provided heat for infracrustal melting to give the more acidic magmas.
This does not, however, imply that subduction was active during the generation of the Sázava suite, as the production of calc-alkaline magmas may post-date the cessation of subduction by as much as 30–50 My (Bonin, 1990). Moreover, as shown above, the majority of the intrusions in the CBP exhibit substantial evidence for mixing of several components. In this plutonic complex, which developed within a relatively short time interval (Holub et al., 1997a), the distinct geochemical characteristics of the individual suites do not have to reflect a major change in the geotectonic environment. In this way, the arc-like geochemical signature of both the orthogneisses (Košler, 1993) and the Sázava suite might have been inherited from a source that could itself be arc related. For instance, the metabasic rocks of the adjacent Jílové zone, whose geochemical signature is compatible with that of a potential source for the Sázava suite, were considered to have originated in a late Proterozoic island-arc setting (Waldhausrová, 1984) as supported by the identification of metaboninites therein (Fediuk, 1992).
Mantle enrichment and generation of the basic magmas
A subduction-related volatile influx, regardless of its timing, may have been responsible for widespread variable enrichment of incompatible elements in the local lithospheric mantle, whose later partial melting led to the generation of basic shoshonitic magmas, isotopically similar to the most basic members of the Blatná and Čertovo břemeno suites. A comparable origin for K-rich intrusions occurring in the Elbe valley and Moldanubian zone has been proposed by Wenzel et al. (1997).
There are two possible mechanisms of mantle enrichment that could have acted independently or in conjunction with one another.
In situ growth of radiogenic Sr and Nd could have followed a single enrichment event that produced a reservoir with a uniform isotopic composition, elevated Rb/Sr and lowered Sm/Nd ratios leading, with time, to higher 87Sr/86Sr and lower 143Nd/144Nd than in the pre-enrichment source. If melting of the mantle at destructive plate margins does not produce major fractionation of Rb/Sr (Ellam & Hawkesworth, 1988) then, given that the minettes with the highest (87Sr/86Sr)350 have 87Rb/86Sr of 3–3·5, it would have taken ∼170–190 Ma for a source with this 87Rb/86Sr to have evolved from an 87Sr/86Sr of 0·705 (i.e. similar to the Sázava suite) to 0·712 (i.e. the initial 87Sr/86Sr of the minettes). Thus the enrichment event could have occurred at ∼500–550 Ma. As mantle melting leads to a decrease in Sm/Nd in the melt relative to the source, TNdCHUR model ages can be also used to constrain a minimum age for the enrichment event. For the minettes, these are close to 1·1 Ga (Janoušek et al., 1995). The observed Sr–Nd decoupling may imply that some of the assumptions concerning Sr behaviour were not fulfilled, and that the enrichment is at least Riphean in age. Alternatively, it may point to a direct recycling of a metasedimentary material or mixing of different mantle sources.
Mantle source with an isotopic composition close to, or more depleted than Bulk Earth, could have been contaminated by a subducted metasedimentary component in a manner invoked for the petrogenesis of Hercynian minettes (Turpin et al., 1988) as well as for granitoids from the Sardinia–Corsica Batholith (Tommasini et al., 1995).
The overall range in Sr–Nd isotopic compositions observed in the CBP may have several explanations. The later CBP magmatism could have tapped mantle zones that had a greater subducted sedimentary component, or it could represent lower degrees of partial melting, which preferentially contained the more fusible subducted components. It can be also explained by movement of the melting zone upwards, from the subducted slab to the metasomatized mantle wedge above the fossil subduction zone.
Alternatively, the mixing of distinct mantle components may have taken place. Mafic melts parental to the Sázava suite could have come from a relatively undepleted (asthenospheric?) mantle source, whose upwelling caused heating of the overlying lithospheric mantle. The rise of isotherms would trigger small-scale partial melting of the enriched lithospheric mantle, and lead to contamination during the ascent of the asthenospheric melt, to produce the progressively more enriched basic end-members of the Blatná and Čertovo břemeno suites.
If the lithospheric mantle were geochemically and isotopically heterogeneous, then it was the more enriched zones that were tapped by the later magmatism. The occurrence of K-rich durbachitic rocks exclusively within the Moldanubian unit is consistent with such a heterogeneity having a lateral distribution. The CBP may therefore record the geochemical complexity of processes operating at the boundary between two distinct lithospheric domains (the Teplá–Barrandian and Moldanubian units).
Role of shoshonitic magmas
The heat introduced by the emplacement of shoshonitic magmas into the crust was likely to have been at least partly responsible for widespread crustal anatexis. This anatexis could have been followed by interaction of acidic and shoshonitic magmas, as documented by the abundance of K-rich mafic microgranular enclaves within numerous intrusions of the CBP as well as by petrographic and geochemical evidence for interaction of granodioritic and monzonitic rocks (e.g. Kozárovice quartz monzonite, see above). The modelling of AFC also shows an important role for a crustal contamination in genesis of the Blatná suite.
Taken together, the nearly contemporaneous Blatná and Čertovo břemeno suites (Holub et al., 1997a,1997b) may have been generated by mixing of different proportions of variably enriched mantle with a crustal component(s). Such a model resembles that of Harmon et al. (1984) and Rock & Hunter (1987) for the genesis of Scottish late Caledonian granitoids in which basic, mantle-derived magmas acted both as parents, undergoing crustal contamination, and as heat sources, facilitating melting.
In the case of the Říčany suite, geochemical and isotopic data are consistent with the input of basic magma into the crust inducing melting of peraluminous lithologies similar to those of the Moldanubian unit. These peraluminous melts did not mix significantly with the basic magmas, and were able to segregate and be emplaced at high crustal levels (Janoušek et al., 1997c).
CONCLUSIONS
A diversity of petrogenetic processes is required to account for the geochemical variability shown by the essentially contemporaneous constituent intrusions of the Central Bohemian Pluton.
Partial melting of metabasites, geochemically and isotopically similar to those occurring in the roof pendants of the CBP, partial melting of a mantle source with an isotopic signature close to Bulk Earth, or mixing of magmas derived from both sources gave rise to the relatively primitive calc-alkaline Sázava suite. Geochemical modelling indicates extensive fractional crystallization of mainly amphibole and plagioclase to produce the intra-suite variation. Either high degrees of fractionation of the Sázava magma, or small degrees of melting of a metabasic source could account for the generation of the Požáry trondhjemite.
The variation shown within the mainly granodioritic Blatná suite can be modelled by AFC with a (Moldanubian) paragneiss as a contaminant and increasing DNd values. The fractionating assemblage is thought to be dominated by amphibole > plagioclase + K-feldspar > biotite (Kozárovice intrusion) and plagioclase > biotite > amphibole >> allanite (Blatná intrusion).
Strongly enriched [(87Sr/86Sr)350 ∼ 0·712, εNd350 ∼ −7) mantle-derived melts that evolved either by closed-system fractional crystallization, or by interaction with leucogranitic magmas, gave rise to the durbachitic Čertovo břemeno suite. The variation in the Sedlčany granite is compatible with small degrees of plagioclase–K-feldspar > biotite–amphibole fractionation, accompanied by limited country-rock assimilation (AFC).
Partial melting of (Moldanubian) metasedimentary lithologies is a likely origin of the granitic rocks of the Říčany suite. The Říčany granite forms a reversely zoned body, whose chemical variation was caused mainly by K-feldspar fractionation at depth before intrusion to a high level.
In the Sázava suite, the basic melts may have provided heat for the crustal melting as well as having mixed and mingled with the tonalitic rocks. Likewise, in the Blatná and Čertovo břemeno suites, the basic melts derived from variously enriched mantle sources have acted both as parents, undergoing crustal contamination, and heat sources, facilitating melting.
Evidence for the operation of subduction during the Hercynian episode in the area of the CBP is equivocal.
There was, with time, a conspicuous shift from a more depleted Sr–Nd isotopic composition and calc-alkaline chemistry towards more evolved K-rich calc-alkaline and shoshonitic rocks, which is interpreted as reflecting the involvement of variously enriched mantle sources in the later suites. Had direct recycling of subducted metasedimentary component into lithospheric mantle been operative, then the subduction could have been as young as mid-Devonian. However, if the radiogenic Sr and unradiogenic Nd composition of the lithospheric mantle was a result of closed-system in situ growth, the enrichment event would have been significantly older.
Geochemical study of granitoid suites alone cannot give unambiguous indications of their true geotectonic setting, especially in a context of a complex orogeny such as that of the Hercynides in Central Europe. Instead, the geochemical character may be inherited from the source rocks.
APPENDIX: EQUATIONS FOR CURVED AFC TRENDS IN 1/Sr–(87Sr/86Sr)i OR 1/Nd–εNdi DIAGRAMS
The following equations characterize curved trends in diagrams of the reciprocal of trace-element concentration versus the initial isotopic composition, formed as a result of changes in either r (rate of assimilation/rate of fractional crystallization)or D (bulk distribution coefficient) during AFC (see Powell, 1984). The numerical calculations were performed using beta version of the R package for Windows 95 (Ihaka & Gentleman, 1996).
Given two segments of the curve, each of which can be approximated by straight lines of slopes S1 and S2, we consider the following cases.
D constant, r variable (r > 0)
r1, r2 assumed, unknown assimilant composition
By choosing other values of D, we can produce a series of pairs of lines, the intersections of which can be joined to form a straight line. This corresponds to the contamination locus of Powell (1984) for any value of D and chosen r1 and r2 (i.e. the contaminant must lie along this trend).
D and assimilant composition assumed, unknown r1, r2
By dividing equation (4) by equation (5), the (1 – D) terms cancel out, and we obtain the ratio of r1/r2, which is independent of D. Having assumed a value of r1, the value of r2 is therefore constrained.
Initial constraints on the possible contaminant composition
r constant (r > 0), D variable
r, D1, D2 assumed, unknown assimilant composition
r and assimilant composition assumed, unknown D1, D2
Initial constraints on the possible contaminant composition
Each of these boundaries represents a fan of straight lines of different slopes, depending on the r values. For r = +∞, they correspond to projections of both segments of the trend. However, for most likely values of r between zero and unity, the slope of these lines changes rapidly from +∞ (vertical; r = 0) to zero (horizontal; r = 1). Thus the field of possible contaminants becomes infinitely large as r approaches zero. Therefore, these equations are of little practical value for delimiting a priori the field of possible contaminants.
*Corresponding author. Present address: Czech Geological Survey, Klárov 3/131, 118 21 Prague 1, Czech Republic. Telephone: +(4202) 581 87 40, ext. 308. Fax: +(4202) 581 8748. e-mail: janousek@cgu.cz
This work was supported by a University of Glasgow Postgraduate Research Scholarship and Czech Grant Agency Postdoctoral Grant 205/97/P113 (V.J.), both of which are gratefully acknowledged. We are indebted to F. Finger, J. Pearce, U. Schaltegger and M. Wilson for their helpful reviews. We also thank A. Dudek, R. M. Ellam, F. V. Holub, B. E. Leake and W. E. Stephens for discussions and comments; H. Maluski for permission to present unpublished 40Ar–39Ar data; J. Gallagher, V. Gallagher, A. Kelly, R. Macdonald, K. Sampson, T. Shimmield and V. Sixta for technical assistance; and the British Council for funding exchange visits. The work at SURRC was supported by the Scottish Universities.
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