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Article

Neogene Alkali Basalts from Central Slovakia (Ostrá Lúka Lava Complex); Mineralogy and Geochemistry

by
Ján Spišiak
1,*,
Roberta Prokešová
2,
Juraj Butek
1 and
Viera Šimonová
1
1
Department of Geography and Geology, Faculty of Natural Sciences, Matej Bel University, Tajovského 40, SK-97401 Banská Bystrica, Slovakia
2
Department of Physical Geography, Geomorphology and Natural Hazards, Institute of Geography, Slovak Academy of Sciences, Štefánikova 49, SK-81473 Bratislava, Slovakia
*
Author to whom correspondence should be addressed.
Minerals 2022, 12(2), 195; https://doi.org/10.3390/min12020195
Submission received: 26 November 2021 / Revised: 28 January 2022 / Accepted: 29 January 2022 / Published: 2 February 2022
(This article belongs to the Special Issue Mineralogy, Petrology and Geochemistry of Minerals and Rocks in the Carpathians)
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Abstract

:
Ostrá Lúka basalts are a product of the final phase of Neogene volcanism in Central Slovakia. Their major and trace elements composition is alkaline, a feature confirmed by light rare earth elements (LREE) relative enrichment and some incompatible trace elements ratios. The basalts contain rare surrounded gabbro cumulates. Their peculiarity is a strong zonation of olivines and clinopyroxene. The significant zonation probably indicates a short stop of the melt at shallow depth. The Sr, Nd and Pb isotope compositions indicate an origin from a moderately depleted mantle source. The mineral and chemical composition of the basalts is similar to the Pannonian basin alkali basalts and the Western and Central Europe alkali basalts.

1. Introduction

All Neogene alkali basalts in the Western Carpathian part of the Carpathian-Panonian Region (CPR) have a similar chemical and mineral composition. The composition of the main rock-forming minerals of alkali basalts of the Carpathian region (olivines, clinopyroxenes) has been extensively studied, focusing on geochemistry and isotopic composition ([1,2,3,4,5,6,7,8,9] and others). In contrast, detailed mineral as well as chemical composition of the basalts of central Slovakia has been studied only marginally (e.g., [5,7,10,11], and others). Volcanological and geochronological studies have been performed in much more detail [12,13,14,15,16,17].
This study focuses on the mineralogy and geochemistry of basalts from the Ostrá Lúka lava complex (Central Slovakia). Our findings can be generalized for the area of the Western Carpathians and/or eventually for the whole Carpathian-Panonian Region (CPR).

2. Geological Settings

Alkali basalt (AB) volcanic activity represents the youngest phase of Cenozoic volcanism of the CPR (Figure 1a, [18]). Products of alkali basalt volcanism in this region are concentrated in four main volcanic fields and numerous scattered necks, lava flows and cinder cones [19]. In Slovakia, the products of volcanism are present in two volcanic areas, the South Slovakia Volcanic Field and the Central Slovakia Neogene Volcanic Field (CSNVF, Figure 1a). In both areas, the basaltic volcanic activity occurred discontinuously between 8.0 and 0.1(?) Ma [20] following the paroxysmal Middle Miocene (17–11 Ma) calc-alkaline volcanic phases [21].
Volcanism in the CSNVF was initiated by back-arc extension related to subduction rollback and a contemporaneous uprise of the asthenospheric mantle [24]. Miocene crustal thinning and horst-and-graben tectonics were accompanied by long-lasting volcanism, climaxing during the Langhian and Serravallian. At that time, predominantly andesitic stratovolcanoes were formed in a mostly terrestrial environment [13,25,26,27]. For the largest CSNVF stratovolcano, Štiavnica Volcano, the time span and main phases of volcanic activity have been redefined by Chernyshev et al. [22] based on K-Ar and Rb-Sr data. Four stages of andesitic volcanism, followed by a fifth rhyolite stage, occurred between the Late Langhian (ca. 15.0 Ma) and Early Tortonian (11.4 Ma). Later on, episodic effusions (not defined as separate volcanic stages) of high alumina basalts and alkali basalts occurred between ca. 8.0 and 0.1(?) Ma.
Ostrá Lúka basalts (OL basalts) are the largest AB complex of the CSNVF, covering an area of about 22 km2. The OL volcano was likely active for a long period of more than one million years in the Upper Miocene (6.6–7.8 Ma), as suggested by previous [26] and new Ar/Ar (whole-rock) dating of basalt (unpublished raw data). Thus, the OL basalts likely represent only an erosion remnant of an initially more extensive volcanic complex formed by several lava flows. At present, the lava complex forms a volcanic plateau situated roughly between Zvolen and Dobrá Niva (Figure 1b).
Basalt plateau thickness up to 40–50 m was established by boreholes GK-8 and KJ-38 [27] and geoelectric profiling. Due to flat topography and relatively smooth relief with slightly incised streams, the outcrops of basalt flows are relatively scarce. Nevertheless, the basalts are occasionally exposed along local terrain edges near Ostrá Luka and Bacurov, where samples of relatively fresh (unweathered) rock were collected (Figure 1b).

3. Analytical Methods

Eight basalt samples were collected from Ostrá Lúka lava complex. All samples had similar textures, structures and mineral composition. Two samples were chosen for a detailed study. Silicate minerals were analysed using electron microprobe JEOL JXA 8530FE at the Earth Sciences Institute in Banská Bystrica under the following conditions: accelerating voltage 15 kV, probe current 20 nA, beam diameter 3–8 µm, ZAF correction, counting time 10 s on peak, 5 s on background. The used standards, X-ray lines and D.L. (in ppm) were as follows: Ca (Kα, 25)—diopside, K (Kα, 44—orthoclase, P (Kα, 41)—apatite, F (Kα, 167)—fluorite, Na (Kα, 43)—albite, Mg (Kα, 41)—diopside, Al (Kα, 42)—albite, Si (Kα, 63)—quartz, Ba (Lα, 72)—barite, Fe (Kα, 52)—hematite, Cr (Kα, 113)—Cr2O3, Mn (Kα, 59)—rhodonite, Ti (Kα, 130)—rutile, Cl (Kα, 12)—tugtupite, Sr (Lα, 71)—celestite.
Whole rock chemical compositions were determined at the ACME Analytical Laboratories (Vancouver, Canada). Total abundances of major element oxides were determined by inductively coupled plasma emission spectrometry (ICP-ES) following lithium metaborate–tetraborate fusion and dilute nitric acid treatment. Loss on ignition (LOI) was calculated from the difference in weight after ignition to 1000 °C. For the total carbon (TOT/C) and sulphur analysis (TOT/S) by LECO analysis, the samples were heated in an induction furnace to >1650 °C, which caused the volatilization of all C and S bearing phases. Vapours were carried through an infrared spectrometric cell wherein the concentrations of C and S were determined by the absorption of specific wavelengths in the infrared spectra (ORG/C = TOT/C minus graphite C and carbonate). Concentrations of trace elements and rare earth elements were determined by ICP mass spectrometry (ICP-MS). Further details are accessible on the web page of the ACME Analytical Laboratories (http://acmelab.com/).
The samples were analyzed for Pb and Sr isotopes using a VG Sector 54 IT thermal ionization mass spectrometer (TIMS) at the Department of Geosciences and Natural Resource Management, University of Copenhagen, Denmark. The powdered samples were dissolved by standard procedures using concentrated HNO3, HCl and HF within SavillexTM beakers on a hotplate at 130 °C for 3 days. A 150Nd/147Sm spike was added beforehand. The isotopic ratios of Sm, Nd, Pb and Sr, and of Sm and Nd isotopic dilution concentrations were determined from separately dissolved powder aliquots using a VG Sector 54 IT Thermal Ionization Mass Spectrometer (TIMS) at IGN. Samples were separated over chromatographic columns charged with 12 mL AG50W-X 8 (100–200 mesh) cation resin, where Sr and REE fractions were collected. REE fractions were further separated over smaller chromatographic columns containing Eichrom’sTM LN resin SPS (Part#LN-B25-S, Lisle, Illinois). Sr cuts were purified applying a standardized 3M HNO3-H2O elution recipe on self-made disposable mini-extraction columns, which consisted of 1mL pipettetips in which we fitted a frit filter to retain 0.2 mL intensively pre-cleaned mesh 50–100 SrSpec™ (Eichrome Inc.) resin. The elution recipe essentially followed that of Horwitz et al. [28], scaled to our needs. Sr was eluted/stripped by pure deionized water and then the eluate was dried on a hotplate. Samarium isotopes were measured in a static multi-collection mode, whereas Nd isotopes were collected in a multi-dynamic routine, both on a triple Ta-Re-Ta filament setting. The measured Nd isotope ratios were normalized to 146Nd/144Nd = 0.7219. The mean value of 143Nd/144Nd ratios for our JNdi standard runs during the period the samples were analyzed amounted to 0.512105 ± 5 (2σ; n = 8). Precision for 147Sm/144Nd ratios is better than 2% (2σ). Chemical separation of Pb from the whole rock samples was performed over conventional glass stem and subsequently miniature glass stem anion exchange columns containing, respectively, 1 mL and 200 L of 100–200 mesh Bio-Rad AG 1 × 8 resin. Pb was analyzed in a static multi-collection mode where fractionation was controlled by repeated analysis of the NBS 981 standard (using values of Todt et al. [29]). The average fractionation amounted to 0.105 ± 0.008% (2 σ, n = 5) per atomic mass unit. Total procedural blanks remained below <200 pg Pb which, compared to >100 ng Pb loads, insignificantly affected the measured Pb isotopic ratios of the samples.

4. Mineralogy

The texture, structure and mineral composition of the basalt samples from the studied lava flows are similar. They are dark gray, non- or low-vesicular and the matrix is microlithic-porphyritic with plagioclase, olivine and pyroxene larger crystals. Common alkaline minerals as nepheline and leucite are occasionally present. Locally, the basalts contain oval coarser-grained gabbro cumulates (up to 5 mm in size) with relatively sharp boundaries (Figure 2a,b). Clinopyroxenes of similar composition in basalts and coarser-grained cumulates suggests that the latter come from co-genetic gabbro cumulates.
Olivine is the dominant phenocryst phase but it is also present in the fine-grained matrix. It is only weakly altered. The larger crystals are subhedral, whereas the smaller ones are euhedral. Olivine is only present at the edge of gabbro cumulates. Olivine is characteristically zoned (Figure 2c,d and Figure 3c). However, it is not a classical oscillatory zoning, but two relatively separate phases. The central parts (cores) of the olivines have a high content of the forsterite component (Fo85), whereas the rims have a significantly lower content of the forsterite component (Fo62, Table 1, Figure 4). This composition reflects a re-equilibration (mainly pressure change) during the formation of the different olivine phases with olivines, with Fo85 probably in equilibrium with a more primitive melt.
The composition of the cores of olivine phenocrysts corresponds to that of olivine from alkali basalts ([10,30,31] and others). The rims have relatively sharp boundaries with the cores and display lower Mg contents (Fo65-60) that suggest a re-equilibration during magma ascent toward the surface (with a likely short-term suspension of the ascent). Such a composition is relatively rare and is probably due to the magmatic alteration of olivine that affects the mineral phases prior to eruption, in the magmatic chamber. Changes in olivine composition also correspond to changes in clinopyroxenes. Clinopyroxene rims have higher Ti/Al ratios compared to the cores, which indicates their formation at lower pressures. Except for the significant change in Mg and Fe contents in olivines during “high temperature corrosion”, only minor changes are observed for the other elements. The Mn and Ca contents decrease with the increase Mg # number in olivine (Figure 5). The Cr and Ni contents in the analysed olivines are very low. High temperature corrosions of olivine have also been studied in detail in recent lavas [32,33]. From the Carpathian region, high temperature corrosion of olivine phenocrysts in basalts from Banat has been described [34]. Groundmass olivines have a composition similar to the rims of olivine phenocrysts.
The clinopyroxene phenocrysts are usually zoned, either showing concentric and rarely sector zoning. The variation between core and rim compositions is not large (Table 2, Figure 3f) and follows the normal fractionation trend; the cores have higher Mg, Si and Cr and lower Fe, Ti, Ca and Al than the rims. But the Cr contents in Cpx in alkali basalts have relatively large variations [3,4]. We did not observe high Ti-augite Cpx phenocrysts that are common in alkali basalts [3,9]. However, the marginal parts of the phenocrysts poikilically enclose a large number of ilmenite grains (Figure 3f). It is probable that the rims of Cpx phenocrysts were originally formed by Ti-augite, which was changed by later processes. Based on a significant change in the Ti/Al ratio but also in the AlIV/AlVI ratio (Figure 6), we assume that basaltic magma stopped for a short time during ascent, then the composition of clinopyroxene rims (and olivine rims as well) changed by reaction with the melt. Decompression probably played a dominant role in the change of the Cpx and Ol composition. The composition of coarse-grained Cpx from gabbro cumulates is similar to the central parts of phenocrysts. Tiny Cpx are often lined with olivine phenocrysts (Figure 3d). The compositions of clinopyroxenes (based on the IMA nomenclature, [35]) are displayed in Figure 4. The majority of analyzed pyroxenes plot in the diopside field, but some plot in the augite field. The composition of clinopyroxene is similar to that of colorless phenocrysts of alkali basalts from western Pannonia Basin with a high Mg # 80–85 [9]. Variations in the Cpx composition are shown in Figure 6. The central parts of clinopyroxene correspond to the composition of porphyritic and megacrystic clinopyroxenes from alkali basalt of the western Pannonian Basin [8,9] but also to other Neogene alkali basalts [3]. The rims of clinopyroxenes have a different composition with a lower Mg # and Al contents.
The presence of orthopyroxene was rarely confirmed under the microscope and was not detected in the analyzed polished thin sections.
Plagioclase occurs as phenocrysts and in the matrix as well (Figure 2e,f). Plagioclase phenocrysts are zoned and often enclose olivine, clinopyroxene, and ilmenite grains (Figure 7a,c). Reverse zoning is manifested by an increase in anorthite content from the cores to the rims (from An53 to An62; Table 3). Plagioclase in the marginal parts of gabbro cumulates has a similar zonation (from An35 to An63, Figure 4f). Mihaliková and Šímová [10] also found this type of zoning in some localities of alkali basalts in Central and Southern Slovakia. The composition of plagioclase is plotted in Figure 8. Locally, tiny dark K-feldspar cumulates were found in the central parts of plagioclase phenocrysts (together with olivine, clinopyroxenes and ilmenite).
The alkali character of the studied basalts is confirmed by the absence of quartz and the presence of nepheline. Nepheline is relatively rare and forms tiny irregular grains. It is found mostly at the contact of plagioclase and clinopyroxenes (Figure 3e). Other accessory minerals are ilmenite and, rarely, apatite.

5. Geochemistry

The Neogene alkali basalts from Central Slovakia have a chemical composition (Table 4) similar to published analyses of basalts from similar localities [5,10,11]. In the TAS classification diagram (Figure 9), the studied basalts fall into the field of basaltic trachyandesite (in the alkali rocks field). The alkali character of basalts and their geotectonic position is also confirmed by the contents of other trace elements. We used various discriminant diagrams for classification [37,38,39] (Figure 10a–c). In all used diagrams the studied basalts correspond to plate alkali basalts from the intracontinental rift. The alkaline character of the studied basalts is also documented by the REE contents, showing a significant enrichment of LREE and a decrease of the contents towards HREE (Figure 11a) and a lack of Eu anomaly. Such a pattern (La/YbN ÷ 10) suggests a lower degree of partial melting. Compared with the OIB average, the alkali basalts from Central Slovakia are slightly enriched in Rb, Ba, Th and K and slightly depleted in the remaining incompatible trace elements (Figure 11c). The analyzed alkali basalts are geochemically similar to other alkali basalts from the Panonian Basin magmatic provinces ([40,41,42] and others).
The Sr and Nd isotopic composition and radiogenic isotopes of Pb were determined in two samples (Table 5). The values of 143Nd/144Nd vs. 87Sr/86Sr isotopic ratio of the studied basalts are scattered around the value 143Nd/144Nd typical for CHUR; 87Sr/86Sr values are lower (Figure 12). Projection points of the studied basalts lie in field II, which indicates that the source material of the rocks was generated from the upper mantle. They have a higher 87Sr/86Sr isotopic ratio than MORB and HIMU. In comparison with the isotopic ratios of similar rocks, the studied basalts fall into the field of Western and Central Europe alkali basalts.
The diagram (Figure 13a) illustrates the isotopic ratio of 208Pb/204Pb vs. 206Pb/204Pb. The studied basalts lie in the field of Pannonian Basin alkali basalts. Compared to the North Hemisphere Reference Line (NHRL), the studied basalts have a relatively lower 207Pb/204Pb ratio. The NHRL represents asthenosphere derived MORB and OIB melts. We also compared the isotope ratios 143Nd/144Nd vs. 206Pb/204Pb of the studied basalts with mantle basic derivatives (Figure 13b). The studied basalts lie outside the MORB, EAR, FOZO and HIMU fields, but they fall into the OIB field.

6. Discussion and Conclusions

The studied basalts are characterized by a strong zonation of Ol and Cpx. Olivines are characterized by a higher content of the forsterite component (Fo85) in the core and a lower content of the fayalite component (Fa60) in the rims. Similarly, Cpx have a significant change in the Ti/Al but also in the AlIV/AlVI ratio (Figure 6) from core to rims. Cpx rims have higher Ti/Al ratios compared to Cpx cores, which indicates their formation at lower pressures. Based on a significant change in olivine and Cpx, we assume that basaltic magma stopped for a short time during its ascent and then the composition with Cpx rims (and also olivine rims) changed by reaction with the melt. The change in pressure (decompression) probably played a dominant role in the change of the Cpx and Ol composition. Olivines with an Fo85 and Cpx core may have been in equilibrium with primitive mantle melts and Ol and Cpx rims’ compositions correspond to the equilibrium of the melt after partial crystallization of the minerals with a short stop of its movement to the surface. We used the formula of Smith et al. [58] to approximate the Cpx crystallization pressure. According to these data, Cpx cores crystallized at higher pressures (0.8 Gpa—approx. 35 km depth) than Cpx rims (0.5 Gpa—approx. 23 km depth) [59].
Various types of cumulates and xenoliths have been described from the Carpathian-Pannonian Region (CPR): spinel peridotites [60,61,62], pyroxenites [63,64], but also granulites [63,65] and other rock types. In the studied basalts, rare small (up to 8 mm) coarse-grained, oval-shaped cumulates are observed. They are mostly composed of Cpx and Plg. The chemical compositions of Cpx and Plg in the cumulates and the host rock are similar; therefore, we assume that these represent a sort of magma cumulates, not xenoliths.
Based on their geochemical composition, we can classify the Neogene olivine basalts from Central Slovakia as intraplate alkali basalts. This setting corresponds to their geological position—they are the result of the Late Tertiary post-orogenic extension of the Pannonian Basin following the Eocene-Miocene subduction. This is evidenced by various discrimination diagrams (Figure 10), but also by the contents of REE and other elements (Figure 11). The contents of these elements correlate well with their contents in the compared basalts from different Carpathian-Pannonian regions [10,11,40].
Isotope compositions of Sr, Nd and Pb confirmed previous findings. From a genetic point of view, the 143Nd/144Nd and 87Sr/86Sr isotopic ratio indicate the origin of these basalts from a moderately depleted mantle source. The 206Pb/204Pb isotopic ratio has a value of about 19, which is higher than MORB but lower than HIMU. The isotope ratios are similar to OIB and to the Pannonian Basin alkali basalts.
Neogene-Quaternary mafic alkalic volcanism in the Carpathian-Pannonian region generally followed calc-alkaline volcanism. In the Central Slovakia Neogene Volcanic Field, alkaline magmas (including those in the studied area) were generated after the termination of calc-alkaline activity (8 Ma to 6.6 Ma), and a second short pulse occurred much later at ca. 0.5 Ma [66] or 0.13–0.14 Ma [67].
Central Slovakia Neogene alkaline magmatism postdated the Middle Miocene crustal thinning, which occurred mostly along the mid-Hungarian belt, where the Alcapa and Tisia-Dacia microplates were in contact since the Early Miocene. Opposite rotations of the microplates may have also contributed to crustal thinning [68]. The Central Slovakia Neogene Volcanic field including Ostrá Lúka basalts was generated by alkaline basaltic volcanism, which was accompanied by limited extensional tectonics [69]. Additional study focused on the geochemistry of alkaline rocks from other Central Slovakia Neogene Volcanic occurrences is needed to confirm these conclusions.

Author Contributions

Conceptualization, J.S. and R.P.; methodology, J.S., J.B.; resources, J.S.; R.P., data curation, J.S., J.B., V.Š.; writing—original draft preparation, J.S., R.P., J.B., V.Š., project administration, V.Š., J.S. All authors have read and agreed to the published version of the manuscript.

Funding

This research was supported by grants VEGA 1/0237/18, APVV 19-0065 and APVV-0146-16.

Data Availability Statement

Not applicable.

Acknowledgments

We thank anonymous reviewers and the editor for their constructive remarks on the manuscript. We acknowledge T. Mikuš for microprobe data acquisition.

Conflicts of Interest

We confirm that the authors have declared no conflict of interest.

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Minerals 12 00195 g001 550
Figure 1. (a) Location of the CSNVF and Ostra Luka (OL) lava complex in the Carpathian-Pannonian Region; (b) Geological map of the OL lava complex and the surrounding area [22,23].
Figure 1. (a) Location of the CSNVF and Ostra Luka (OL) lava complex in the Carpathian-Pannonian Region; (b) Geological map of the OL lava complex and the surrounding area [22,23].
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Figure 2. Photomicrograph: (a) contact of basalts with cumulates, parallel polaroids, (b) the same, crossed polaroids, (c,d) zonal olivines, crossed polaroids, (e,f) plagioclase phenocrysts, crossed polaroids.
Figure 2. Photomicrograph: (a) contact of basalts with cumulates, parallel polaroids, (b) the same, crossed polaroids, (c,d) zonal olivines, crossed polaroids, (e,f) plagioclase phenocrysts, crossed polaroids.
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Figure 3. (a,b) Back scattered electron (BSE) images of olivines, clinopyroxenes and plagioclases; (c) BSE image of zonedg olivines (the same as Figure 2c); (d) detail of rims of olivines; (e) BSE image of olivines, clinopyroxenes and plagioclases, (f) BSE image of zonal Cpx; (Pl—plagioclase, Ol—olivine, Cpx—clinopyroxene, Ilm—ilmenite, Ne—nepheline); the numbers in figures correspond to those in Table 1, Table 2 and Table 3.
Figure 3. (a,b) Back scattered electron (BSE) images of olivines, clinopyroxenes and plagioclases; (c) BSE image of zonedg olivines (the same as Figure 2c); (d) detail of rims of olivines; (e) BSE image of olivines, clinopyroxenes and plagioclases, (f) BSE image of zonal Cpx; (Pl—plagioclase, Ol—olivine, Cpx—clinopyroxene, Ilm—ilmenite, Ne—nepheline); the numbers in figures correspond to those in Table 1, Table 2 and Table 3.
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Figure 4. Classification diagram of clinopyroxenes [35], and olivines, D—diopside, H-hedenbergite, A—augite; c—core, r—rims, sample: 1—PLKBR-2, 2—PLKOL-1; 3—gabbro cumulates.
Figure 4. Classification diagram of clinopyroxenes [35], and olivines, D—diopside, H-hedenbergite, A—augite; c—core, r—rims, sample: 1—PLKBR-2, 2—PLKOL-1; 3—gabbro cumulates.
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Figure 5. Plot of Ca and Mn vs. Mg—number in olivine from alkaline basalts (this study); c—core, r—rims.
Figure 5. Plot of Ca and Mn vs. Mg—number in olivine from alkaline basalts (this study); c—core, r—rims.
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Figure 6. Variation of Mg# vs. Ti (a) Al (b) in clinopyroxene; (c,d) Plot of Ti vs. Al and AlIV vs. AlVI [36], symbols as in Fig 4. Field for pyroxene of alkaline basalts from the western Pannonian basin; according to Jankovic et al. [8].
Figure 6. Variation of Mg# vs. Ti (a) Al (b) in clinopyroxene; (c,d) Plot of Ti vs. Al and AlIV vs. AlVI [36], symbols as in Fig 4. Field for pyroxene of alkaline basalts from the western Pannonian basin; according to Jankovic et al. [8].
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Figure 7. (a–d) Back scattered electron (BSE) images of plagioclases, (e,f) BSE image of gabbro cumulates; (Pl—plagioclase, Ol—olivine, Cpx—clinopyroxene, Ilm—ilmenite); the numbers in figures correspond to those in Table 1, Table 2 and Table 3.
Figure 7. (a–d) Back scattered electron (BSE) images of plagioclases, (e,f) BSE image of gabbro cumulates; (Pl—plagioclase, Ol—olivine, Cpx—clinopyroxene, Ilm—ilmenite); the numbers in figures correspond to those in Table 1, Table 2 and Table 3.
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Figure 8. Classification diagram of feldspars; 1—PLKBR-2, 2—PLKOL-1; 3—gabbro cumulates, c—core, r—rims.
Figure 8. Classification diagram of feldspars; 1—PLKBR-2, 2—PLKOL-1; 3—gabbro cumulates, c—core, r—rims.
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Figure 9. TAS diagram for studied basalts [43]; dashed line according to Irvin & Baragar [44], 1—studied basalts.
Figure 9. TAS diagram for studied basalts [43]; dashed line according to Irvin & Baragar [44], 1—studied basalts.
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Figure 10. Discrimination diagram for basalts: (a) Th-Hf-Ta [37]; (b) Zr-Ti-Y [38], The fields are defined as follows: N-MORB—normal Mid Ocean Ridge Basalt; E-MORB—enriched Mid Ocean Ridge Basalt; WPT—within-plate tholeiites, WPA—within-plate alkaline basalts, CAB—calc-alkaline volcanic arc basalts, IAT—island arc tholeiites. The broken lines indicate transitional zones between basalt types. (c) La-Y-Nb [39], field: 1A—CAB, 1C—volcanic arc tholeiites, 1B—overlap between 1A and 1C, 2A—continental basalts, 2B—back-arc basin basalts, 3A—WPA, 3B, 3C—E-MORB, 3D—N-MORB.
Figure 10. Discrimination diagram for basalts: (a) Th-Hf-Ta [37]; (b) Zr-Ti-Y [38], The fields are defined as follows: N-MORB—normal Mid Ocean Ridge Basalt; E-MORB—enriched Mid Ocean Ridge Basalt; WPT—within-plate tholeiites, WPA—within-plate alkaline basalts, CAB—calc-alkaline volcanic arc basalts, IAT—island arc tholeiites. The broken lines indicate transitional zones between basalt types. (c) La-Y-Nb [39], field: 1A—CAB, 1C—volcanic arc tholeiites, 1B—overlap between 1A and 1C, 2A—continental basalts, 2B—back-arc basin basalts, 3A—WPA, 3B, 3C—E-MORB, 3D—N-MORB.
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Figure 11. Spider diagrams for analyzed basalts: (a) Rare earth elements normalised to chondrite [45], (b) Rare earth elements normalised to OIB (ocean island basalt) [46], (c) incompatible trace element abundances normalised to OIB [46]. Gray fields represent analyses of Neogene alkali basalts from different Carpathian-Pannonian regions [10,11,42].
Figure 11. Spider diagrams for analyzed basalts: (a) Rare earth elements normalised to chondrite [45], (b) Rare earth elements normalised to OIB (ocean island basalt) [46], (c) incompatible trace element abundances normalised to OIB [46]. Gray fields represent analyses of Neogene alkali basalts from different Carpathian-Pannonian regions [10,11,42].
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Figure 12. 143Nd/144Nd vs 87Sr/86Sr discriminant diagram. Sr and Nd isotope variations of studied alkaline basalts compared with fields of alkaline basalts from the Pannonian Basin basalts [40,47] and from alkaline basalts from Western and Central Europe [48]. HIMU (high μ refers to high 238U/204Pb), BSE (Bulk Silicate Earth) according Lustrino and Wilson [49]; CHUR (chondrite uniform reservoir); OIB (oceanic island basalt) according to Faure [50], 1—studied basalts.
Figure 12. 143Nd/144Nd vs 87Sr/86Sr discriminant diagram. Sr and Nd isotope variations of studied alkaline basalts compared with fields of alkaline basalts from the Pannonian Basin basalts [40,47] and from alkaline basalts from Western and Central Europe [48]. HIMU (high μ refers to high 238U/204Pb), BSE (Bulk Silicate Earth) according Lustrino and Wilson [49]; CHUR (chondrite uniform reservoir); OIB (oceanic island basalt) according to Faure [50], 1—studied basalts.
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Figure 13. (a) 208Pb/204Pb vs 206Pb/204Pb discriminant diagram; dashed line—field alkali basalts from Western and Central Europe [47], NHRL from Hart [51], (b) 143Nd/144Nd vs 206Pb/204Pb diagram: mantle components (FOZO, HIMU)—from Zindler and Hart [52], EAR—from Cebriá & Wilson [53], OIB and MORB—data from Ghatak and Basu [54], Jackson and Dasgupta [55], Blasise et al. [56] and Sommer et al. [57], 1—studied basalts.
Figure 13. (a) 208Pb/204Pb vs 206Pb/204Pb discriminant diagram; dashed line—field alkali basalts from Western and Central Europe [47], NHRL from Hart [51], (b) 143Nd/144Nd vs 206Pb/204Pb diagram: mantle components (FOZO, HIMU)—from Zindler and Hart [52], EAR—from Cebriá & Wilson [53], OIB and MORB—data from Ghatak and Basu [54], Jackson and Dasgupta [55], Blasise et al. [56] and Sommer et al. [57], 1—studied basalts.
Minerals 12 00195 g013aMinerals 12 00195 g013b
Table
Table 1. Chemical composition of olivines.
Table 1. Chemical composition of olivines.
SamplePLK BR-2PLKOL-1PLK BR-2PLKOL-1
Ana No12345678910111213141516171819202122
Figures3a3a3a3a3b3b3b3c3c3c3c3c3c3c3e3e3e3f4c4d4e4e
SiO237.5736.2435.9235.7438.3536.6937.8839.6040.2539.7836.8836.9836.8036.8735.8235.6536.1336.0637.5536.3537.5237.50
TiO20.020.040.060.040.020.040.030.090.030.110.070.160.090.020.120.060.040.010.030.100.000.02
Al2O30.000.020.050.030.030.010.070.090.050.030.010.010.030.030.000.010.000.030.150.040.020.02
Cr2O30.020.000.000.000.000.010.000.000.000.000.000.000.000.000.020.000.000.010.090.000.020.02
FeO *26.5332.7735.5934.7022.9031.4323.9014.5014.2714.2631.7631.9131.7332.7236.3135.4134.7933.0934.4934.5528.5028.05
MnO0.490.700.870.850.380.670.460.140.120.190.490.530.460.620.850.810.860.600.320.730.390.37
CaO0.220.350.370.360.210.350.210.220.200.200.320.310.340.300.410.380.370.340.510.660.340.27
MgO35.3830.1727.1527.6137.9330.8937.2344.5044.9844.4130.3429.9930.4529.1826.5927.1928.4928.5826.2327.1432.8333.37
NiO0.000.000.000.020.070.000.060.000.000.000.000.000.000.000.000.000.,000.000.000.000.000.00
Na2O0.000.030.050.000.060.020.000.030.000.030.020.000.030.000.010.080.060.040.000.070.000.00
K2O0.000.000.000.000.000.010.000.000.000.000.000.000.000.000.000.010.000.000.000.000.000.00
Total100.22100.32100.0699.3599.94100.1199.8499.1799.9099.0099.8999.8999.9499.75100.1399.61100.7398.7599.3899.6399.6099.60
Formula based on 4 oxygens
Si0.9960.9921.0031.0011.0031.0000.9961.0021.0091.0081.0101.0151.0071.0181.0041.0000.9961.0091.0571.0181.0141.010
Ti0.0000.0010.0010.0010.0000.0010.0010.0020.0010.0020.0020.0030.0020.0000.0030.0010.0010.0000.0010.0020.0000.000
Al0.0000.0010.0020.0010.0010.0000.0020.0030.0010.0010.0000.0000.0010.0010.0000.0000.0000.0010.0050.0010.0010.001
Cr0.0000.0000.0000.0000.0000.0000.0000.0000.0000.0000.0000.0000.0000.0000.0010.0000.0000.0000.0020.0000.0000.000
Fe3+0.0070.0150.0000.0000.0000.0000.0050.0000.0000.0000.0000.0000.0000.0000.0000.0000.0070.0000.0000.0000.0000.000
Fe2+0.5810.7350.8310.8130.5010.7170.5210.3070.2990.3020.7280.7330.7260.7560.8510.8310.7950.7740.8120.8090.6440.632
Mn0.0110.0160.0210.0200.0080.0150.0100.0030.0030.0040.0110.0120.0110.0140.0200.0190.0200.0140.0080.0170.0090.008
Mg1.3981.2311.1311.1531.4801.2561.4601.6781.6821.6781.2391.2271.2431.2011.1101.1371.1711.1921.1001.1331.3221.340
Ca0.0060.0100.0110.0110.0060.0100.0060.0060.0050.0050.0090.0090.0100.0090.0120.0110.0110.0100.0150.0200.0100.008
End members (%)
Fo69.78961.32156.71257.73874.16462.84272.93084.16384.55684.34062.35361.94162.45660.66255.70156.90358.43959.88156.85957.24566.62067.408
Fa29.35437.35541.70540.71225.12235.86626.26315.38715.04715.19036.60836.97636.50638.15942.68141.56740.02338.90341.94840.88132.44331.782
FeO * total Fe as FeO.
Table
Table 2. Chemical composition of clinopyroxenes.
Table 2. Chemical composition of clinopyroxenes.
SamplePLKBR-2PLKOL-1PLKBR-2PLKOL-1Gabbro Cumulates
Anal. No.123456789101112131415
Figures3a3a3d3d3d3e3e3f3f4c4c4d4f4f4f
SiO247.9750.3249.6148.7851.6750.4050.8949.4348.8149.4449.6351.6851.9148.8349.84
TiO22.191.692.252.761.591.751.601.612.021.531.551.361.231.491.22
Al2O36.843.453.244.282.162.472.216.605.286.216.992.421.947.616.83
Cr2O30.060.060.020.000.000.000.010.250.020.100.080.000.070.200.92
FeO *7.987.7510.259.508.658.588.256.017.867.235.868.758.295.524.63
MnO0.140.200.250.290.220.210.230.180.210.190.080.200.210.210.07
CaO21.0221.7420.6821.3021.3221.8721.8920.5521.7620.3620.5621.3421.4020.7120.48
MgO13.1414.2913.1812.5713.9414.1614.3014.5513.4414.3214.6713.6914.1614.2914.77
Na2O0.630.470.370.490.340.450.510.390.350.460.480.420.400.520.50
K2O0.010.020.000.000.000.030.020.000.000.000.000.000.000.000.00
Total99.9899.9999.8499.9899.8999.9299.9199.5799.7599.8599.9099.8699.6199.3799.27
Formula based on 6 oxygens
Si1.7791.8661.8641.8301.9301.8771.8931.8261.8191.8271.8231.9301.9391.8021.839
Ti0.0610.0470.0640.0780.0450.0490.0450.0450.0570.0430.0430.0380.0350.0410.034
Al0.2990.1510.1430.1890.0950.1090.0970.2870.2320.2710.3030.1060.0850.3310.297
Cr0.0020.0020.0000.0000.0000.0000.0000.0070.0010.0030.0020.0000.0020.0060.027
Fe3+0.0640.0550.0270.0300.0000.0720.0650.0000.0430.0210.0000.0000.0000.0130.000
Fe2+0.1830.1850.2950.2680.2700.1960.1920.1860.2020.2030.1800.2730.2590.1580.143
Mn0.0040.0060.0080.0090.0070.0070.0070.0060.0070.0060.0020.0060.0070.0070.002
Mg0.7260.7900.7380.7030.7760.7860.7930.8020.7470.7890.8030.7620.7880.7870.813
Ca0.8350.8640.8330.8560.8530.8730.8720.8140.8690.8060.8090.8540.8560.8190.810
Na0.0450.0340.0270.0360.0250.0320.0370.0280.0250.0330.0340.0300.0290.0370.036
End members (%)
Wo46.17445.59743.97546.10444.91345.30845.39045.17846.69744.33545.14145.20144.98546.10945.869
En40.14241.70939.00737.84940.86740.81341.25444.50440.13243.37044.82240.33041.40944.28946.032
Fs13.68412.69417.01816.04714.22013.87813.35610.31813.17112.29410.03714.46913.6069.6028.099
Mg#0.7980.810.7140.7240.7420.8010.8050.8120.7870.7960.8170.7360.7530.8330.85
FeO * total Fe as FeO.
Table
Table 3. Chemical composition of plagioclases.
Table 3. Chemical composition of plagioclases.
SamplePLKBR-2PLKOL-1Gabbro Cumulates
Anal N.123456789101112131415
Figures3a3a3e3e4b4b4b4c4c4c4c4d4d4f4f
SiO257.3753.9354.2065.4455.8652.5057.8353.2956.0752.0052.6463.1662.5458.6851.42
TiO20.000.000.000.000.000.000.000.220.060.,000.220.090.210.190.17
Al2O326.0728.6628.1219.7027.3429.5925.6429.4227.0030.0728.9321.2821.6524.6529.21
FeO *0.630.380.750.330.370.370.840.180.290.300.660.250.300.480.44
MnO0.000.000.000.000.000.000.000.070.000.020.040.020.000.080.00
CaO9.1811.9611.701.6010.5912.898.1512.029.0812.7911.902.813.357.0712.48
MgO0.000.020.010.000.030.020.060.030.020.050.020.010.020.020.06
BaO0.000.000.000.000.000.000.000.010.060.000.020.040.190.070.00
SrO0.110.140.170.050.170.160.070.090.170.180.220.130.110.170.22
Na2O5.594.264.436.374.893.896.244.405.914.064.427.247.306.713.83
K2O0.550.330.315.910.450.260.730.290.590.220.274.283.500.890.30
99.4999.6799.6899.4099.7099.6899.56100.0199.2599.6999.3399.3099.1799.0198.13
Formula based on 8 oxygens
Si2.6082.4622.4752.9602.5432.3992.6142.4192.5452.3712.4112.8442.8232.6642.389
Ti0.0000.0000.0000.0000.0000.0000.0000.0070.0020.0000.0080.0030.0070.0060.006
Al1.3971.5421.5141.0501.4671.5941.3661.5741.4441.6161.5611.1291.1511.3191.,600
Cr0.0000.0000.0000.0000.0000.0000.0000.0000.0000.0000.0000.0000.0000.0000.000
Fe3+0.0000.0000.0000.0000.0000.0000.0000.0000.0000.0000.0000.0000.0000.0000.000
Fe2+0.0240.0140.0290.0120.0140.0140.0320.0070.0110.0110.0250.0090.0110.0180.017
Mn0.0000.0000.0000.0000.0000.0000.0000.0030.0000.0010.0010.0010.0000.0030.000
Mg0.0000.0010.0000.0000.0020.0020.0040.0020.0010.0040.0010.0000.0010.0010.004
Ca0.4470.5850.5720.0780.5170.6310.3950.5850.4420.6250.5840.1360.1620.3440.621
Ba0.0000.0000.0000.0000.0000.0000.0000.0000.0010.0000.0000.0010.0030.0010.000
Na0.4920.3770.3920.5590.4320.3440.5470.3870.5200.3590.3930.6320.6390.5910.345
K0.0320.0190.0180.3410.0260.0150.0420.0170.0340.0130.0160.2460.2020.0520.017
End members (%)
An46.04959.62458.2607.93053.02763.71240.11559.14044.32562.69358.85913.38716.16734.86663.136
Ab50.68938.40639.91657.19544.30034.75355.58439.19052.22936.03839.57562.37163.72959.89035.086
Or3.2611.9701.82534.8752.6721.5364.3021.6703.4461.2691.56624.24220.1055.2441.778
FeO * total Fe as FeO.
Table
Table 4. Chemical composition of rocks.
Table 4. Chemical composition of rocks.
SamplePLKOL-01PLKBR-02SamplePLKOL-01PLKBR-02SamplePLKOL-01PLKBR-02
SiO251.3250.16Sc16.015.00Y21.0023.80
TiO22.002.26Ba379.00406.00La27.6029.10
Al2O317.1917.60Be2.002.00Ce55.1060.10
Fe2O3*9.709.42Co36.7027.90Pr6.477.22
FeO Cs0.800.90Nd25.4028.10
Cr2O30.01< 0.002Ga18.3019.20Sm5.315.68
MnO0.160.14Hf4.705.00Eu1.641.84
CaO7.557.20Nb37.0040.90Gd5.165.58
MgO5.474.16Rb47.4049.50Tb0.720.80
Na2O4.374.37Sn2.003.00Dy4.154.52
K2O1.912.16Sr559.10594.30Ho0.760.83
P2O50.370.41Ta2.502.50Er1.992.16
LOl0.301.80Th5.305.40Tm0.290.32
Total100.3599.68U1.701.60Yb1.781.91
V167.00179.00Lu0.270.30
TOT/C0.030.02W10.109.50Ni58.00<20
TOT/S<0.02<0.02Zr199.90220.50
Fe2O3* total Fe as Fe2O3.
Table
Table 5. Isotope composition of rocks.
Table 5. Isotope composition of rocks.
SamplePLKOL-01PLKBR-02
phasewhrwhr
206Pb/204Pb18.95045818.944746
± 2s+0.0108180.009048
207Pb/204Pb15.64266815.634560
± 2s+0.0107570.009456
208Pb/204Pb38.99435638.962283
± 2s+0.0317870.028764
207Pb/206Pb0.8254520.825273
± 2s+0.0001740.000155
208Pb/206Pb2.0577092.056636
± 2s+0.0007530.000689
87Sr/86Sr0.7035690.703586
± abs0.0000040.000006
143Nd/144Nd0.5127790.512818
± abs0.0000060.000006
Nd26.3527.62
Sm5.756.07
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Spišiak, J.; Prokešová, R.; Butek, J.; Šimonová, V. Neogene Alkali Basalts from Central Slovakia (Ostrá Lúka Lava Complex); Mineralogy and Geochemistry. Minerals 2022, 12, 195. https://doi.org/10.3390/min12020195

AMA Style

Spišiak J, Prokešová R, Butek J, Šimonová V. Neogene Alkali Basalts from Central Slovakia (Ostrá Lúka Lava Complex); Mineralogy and Geochemistry. Minerals. 2022; 12(2):195. https://doi.org/10.3390/min12020195

Chicago/Turabian Style

Spišiak, Ján, Roberta Prokešová, Juraj Butek, and Viera Šimonová. 2022. "Neogene Alkali Basalts from Central Slovakia (Ostrá Lúka Lava Complex); Mineralogy and Geochemistry" Minerals 12, no. 2: 195. https://doi.org/10.3390/min12020195

APA Style

Spišiak, J., Prokešová, R., Butek, J., & Šimonová, V. (2022). Neogene Alkali Basalts from Central Slovakia (Ostrá Lúka Lava Complex); Mineralogy and Geochemistry. Minerals, 12(2), 195. https://doi.org/10.3390/min12020195

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