Red sandstone as raw material of Baden culture (Late Copper Age) grinding stones (Balatonőszöd-Temetői dűlő site, Hungary), with a review of the red sandstone formations of SW Hungary

Balatonőszöd Temetői dűlő is one of the largest excavated and longest-lived sites of the Late Copper Age Baden Culture in Hungary, where 500 lithic finds were registered. In the site finds belonging to the late Middle Copper Age Balaton-Lasinja Culture and the Late Copper Age Boleraz Culture were found too. This paper presents petrographic and geochemical analyses of stone utensils, mostly of grinding stones, made of red, or discoloured white sandstones. Almost all sandstone artefacts are upper and lower stones of grinding equipment and polishers, as well as objects whose function is not known, worked and non-worked fragments; boulders of raw material are also in the studied set. The detailed petrographic and geochemical methods applied here are polarized light microscopy and a distribution study of the framework grains in thin section, and ICP-OES and ICP-MS as bulk rock chemical methods. The results were compared to published petrographic and geochemical data. Most of the studied artefacts were made of the rocks of the Red Sandstone and Siltstone Member of the Balaton Highland Sandstone Formation, especially from the mature type sandstone in which quartz is predominant, and which is almost free of feldspar. This type is characteristic of the confines of the Southern Balaton Highland and the lower part of the formation in the Northern Balaton Highland. A minor part of the studied artefacts red or purple, purplish grey sandstones originates from the sandstones of the Jakabhegy Sandstone Formation (Western Mecsek mountains).

flourishing time lasted for almost 500 years (3330-2860 cal. BCE, the latest measured date was 2740-2590 cal. BCE). On the site, features of the late Middle Copper Age Balaton-Lasinja Culture (3950-3690 cal. BCE) and the Late Copper Age Boleraz Culture (formerly known as the Boleraz phase of the Baden Culture, 3470-2900 cal. BCE) were also found. Some features of the three cultures occurred together (mixed) though no traces of any later digging in or upsetting could be observed in the section (Horváth 2010;2014;Horváth et al. 2006).  (Horváth et al. 2006, modified, original aerial photo and picture by Zsolt Viemann) the matrix and the cementation is very small in comparison to the mineral grains. On the basis of their colour this group has been divided into two subgroups: Subgroup I/1 (131 specimens): in general, they are typical red sandstones, but there are also orange-red, purplish-red (and darker, with a greyish shade) species in this subgroup. (Figure 2a). Figure 2. (Group I) Macroscopic photos: a) red sandstone (Subgroup I/1). b) partly discoloured red sandstone (transition between Subgroup I/1 and I/2). c) discoloured "red" sandstone (Subgroup I/2). Subgroup I/2 (52 specimens): in general, these sandstones are discoloured, they are light coloured (a pale shade of grey to almost white), with -sporadically -faintly reddish, orangered, occasionally yellow or purplish-grey coloured patches of weathering. (Figure 2c).
The originally red colour of the discoloured specimens clearly shows in ten of the examined finds that have both red and "white" (i.e., a pale shade of grey, discoloured) parts. These pieces have been assigned to Subgroup I/1. (Figure 2b). The discolouration (bleaching) of red sandstones is a well-known feature in geological deposits of the Balatonfelvidék Sandstone Formation (see section 4.1.), but in the case of an artefact we cannot exclude postdepositional alterations.

Group II (5 pieces)
Group II comprises purplish grey, purple, red mottled, coarse-or medium-grained, clastsupported sandstones. Quartz is their main component. Among the coarse sand grains, there are poorly rounded quartz-and quartzite-pebbles, with a maximum size of 1.5 cm. White or occasionally pale red, angular feldspar-grains, not bigger than 1 mm, are also observable. The appearance of the detrital micas occurring in this group is similar to the ones in Group I, but in smaller quantities and smaller sizes than those in Group I (Figure 3). (2020)

Group I
In thin section, the two subgroups do not differ from each other at all. The grains -as a whole -are unrounded or only slightly subangular.    Quartz prevail among the grains, but polycrystalline quartz is also present in great quantity. The quantity of the volcanic rock fragments is higher than the quantity of metamorphic clasts. An important feature is the total absence of feldspars. The cement is limonitic-hematitic (which causes the red, occasionally orange or purplish colour of the rock when examined macroscopically), siliceous or carbonatized (possibly secondarily). Chalcedony -though very rarely -is also observable (Figure 7b). The porosity of the samples is insignificant, their fabric is compact. The few pores and interstices are mainly filled with chalcedony during lithification, though chlorite filling also occurs.

Group II
Constituents: -clastic, unrounded (or only slightly rounded) quartz grains ( Figure 8); -generally rounded polycrystalline quartz grains ( Figure 8); -detrital micas (muscovite and discoloured, chloritized biotite; Figure 9); -rock fragments (volcanic): grains with felsitic texture (Figure 10a) and spherulitic volcanic glass clasts ( Figure 10b); -rock fragments (metamorphic): deformational fabric (banded) polycrystalline quartzite-rock lithoclasts; -feldspars (plagioclase and microcline; Figure 11a    Major constituents are monocrystalline and polycrystalline quartz grains. The appearance of the detrital micas is similar to the ones in Group I, but in smaller quantities and smaller grain size. The size and quantity of the magnetite grains are also smaller than in Group I. Characteristic features -compared to Group I -are the presence of feldspars and of siltstone lithoclasts. Practically, there is no matrix, the fabric of the rock is even more packed than in Group I, however, limonitic fillings of cavities occur (Figure 8b).

Distribution of the framework grains
On the basis of the proportion of the clastic constituents, the studied members of Subgroup I/1 and I/2 are lithic arenites (litharenites) and sublitharenites and the studied members of Group II are classified as a transitional composition between subarkoses and sublitharenites.

Results -Bulk rock chemistry
The bulk rock chemical data (ICP-OES and ICP-MS results) of the studied artefacts and recently gathered red sandstone comparative samples (from the Balaton Highland) are presented in Tables 1-4.

Possible source regions -red sandstones in Hungary
There are many sandstone formations on the surface in SW-Hungary, but only a few have red colour -so we have to investigate these formations for the raw material sources.
So far, in the Hungarian archaeological assemblages only a few sandstone artefacts were studied archaeometrically (Palágyi et al. 2006;Piros 2010;Szakmány 1996 Szakmány et al. 2008), therefore it is important to give the whole set of information about these formations, as they represent potential raw materials.

The Balaton-Highland
Balatonfelvidék Sandstone Formation (Upper Permian age): Rocks of the Balatonfelvidék Sandstone Formation (a.k.a. "Permian red sandstone") crop out close to the archaeological site, on the opposite (northern) side of the lake Balaton on the Balaton-Highland (see Figure 12) in a 12 km long, and 5 km wide area between Zánka and Badacsonyörs, a 22 km long and maximum 3 km wide area between Aszófő and Balatonfűzfő, and in some small places near Gyulakeszi, Hidegkút and Litér (Csernussi 1984;Fülöp 1990;Majoros 1963;. This Permian age fluvial sequence consists of three members. The lower member (Paloznak Phanglomerate Member) is a sporadically red coloured, coarse-grained, polymict breccia which originated from semiarid climate talus cones. On the basis of the formation, the Badacsonyörs Conglomerate Member is prevalent, with pebbles and gravels originating from the Balaton Phyllite Formation-Group (the siltstone-shale pebbles and sandstone-shale pebbles) and from the Kékkút Dacite Formation (the red and grey pebbles), and a few siliceous shale-, limestone-, gneiss-pebbles. The most prevalent member is the Red Sandstone and Siltstone Member: an alternation of red sandstone and siltstone, with frequent intercalations of intraformational conglomerate beds. Grey coloured sandstone occurs on the fringe territories of the formation and the lower parts of the member, and in some intraformational conglomerate beds (Csernussi 1984;Fülöp 1990;Majoros 1963;.
The proportion of the clastic constituents is monotonic: dominant phases are quartz and rock fragments, micas (muscovite, biotite), and "more or less, or zero amount of feldspars" (Fülöp 1990). Among the rock fragments Lower Palaeozoic siltstone, sandstone and metamorphozed acidic volcanic rock fragments occur, together with dacite from the Kékkút Dacite Formation. Quartz-phyllite and gneiss are also present, but only in small quantities. Intraformational siltstone-and dolomite-fragments are also detectable (Csernussi 1984;Fülöp 1990;Majoros 1963;.
The amount of feldspars is less than 20% (acidic plagioclase, infrequently orthoclase and microcline), the feldspars are frequently sericitizated, and infrequently kaolinizated (Csernussi 1984;Fülöp 1990;Majoros 1963;. Micas are regularly present: muscovite and discoloured, chloritized biotite. Illite and kaolinite are the most frequent clay minerals (Fülöp 1990). The cementation is most frequently sericitic or illitic with a dispersed distribution of hematite (and a subordinate amount of gypsum, anhydrite or magnesite displacing sericite). Hematite often occurs as a crust on the clastic grains too. On the basin margins, in the mature sandstones, the cement is composed of microcrystalline quartz together with kaolinite and dispersed hematite. Infrequently dolomite, gypsum, anhydrite and magnesite occur as independent cement material (Fülöp 1990).
The sandstones of the Balatonfelvidék Sandstone Formation can be divided into two lithological facies types. The dominant facies type is a poorly matured sandstone with bimodal grain-size distribution, quartz, rock fragments and feldspar as clastic constituents and with an illitic-sericitic (or dolomitic) matrix (Fülöp 1990).
The second facies type is a specific feature of the southern Balaton-Highland's fringe territories and of the northern Balaton-Highland, on the lower parts of the formation. It is a mature sandstone type with unimodal grain-size distribution, the clastic constituents are quartz and rock fragments (feldspars are almost absent). The cementation is microcrystalline quartz with kaolinite (Fülöp 1990).
Primary porosity usually vanished by compaction in all types (Csernussi 1984). Grey (discoloured) medium-and coarse-grained variants are present in the south-western part of the area of the formation (and in a local development at the Hajógyári quarry at Balatonfüred). At the Örsi-hill (near Badacsonyörs, also in the south-western part of the area) crops out a sequence of on the upper side red and on the lower side grey siltstone and sandstone bands, between the lower grey, medium-and coarse-grained sandstone bands and the upper red, fine-grained sandstone bands (Csernussi 1984).

The Western Mecsek mountains
Permian -Lower Triassic clastic sequences of red conglomerates, sandstones and siltstones are typical in the Western Mecsek mountains, with a wide surface area (see Figure  Journal of Lithic Studies (2020) (Figure 12). The oldest -Lower Permian -Korpád Sandstone Formation is mostly known from drilling cores with a thickness of 100-700 m and with a few surface outcrops (Budai & Gyalog 2010;Gyalog 2005). This formation consists of dominantly red, clastic sediments with a significant refinement in the grain size upwards in the sequence (from conglomerate to sandy siltstone). Most of the grains of the conglomerates and sandstones are quartz, quartzite, metamorphic-and volcanic rock fragments (Barabás & Barabás-Stuhl 1998).
Feldspars are mostly represented by plagioclases, but the secondary albitization of the Kfeldspar grains cannot be excluded (Varga 2009). Potassium-feldspars and plutonic rock fragments are absent or present only in very small amounts within the clastic constituents (Fazekas 1987). Micas are muscovite and strongly chloritized biotite (Varga 2009).
Among the volcanic rock fragments those with andesitic composition are frequent (sporadically fluidal texture with plagioclase microlithes and opaque minerals). This type is unique in the whole sequence in the Western Mecsek mountains and differs from the acidic volcanic rock fragments which originate from the Lower Permian Gyűrűfű Rhyolite Formation (Barabás & Barabás-Stuhl 1998;Fazekas 1987;Varga 2009). This type of rock fragments is also missing among the studied artefacts.
The Upper Permian Cserdi Formation has a 1000 m average thickness and only a few small outcrops near Gyűrűfű, Dinnyeberki, Cserdi and Boda. This fluvial sequence consists of the rhythmical alternation of reddish brown (or brownish red, or purplish red) conglomerates and coarse-grained sandstones together with silty fine-grained sandstones in subordinate quantities, with a significant refinement in the grain size upwards in the sequence (Barabás & Barabás-Stuhl 1998;Bodor & Szakmány 2009). The rocks of this formation are usually unsorted, and it is characteristic that the coarse-grained bands have a large amount of matrix (silt and fine-grained sand). Totally unsorted, predominantly fine-grained sandstone is also frequent in the sequence. This type of sandstone consists of unrounded, some mm-sized sand grains or very fine, subangular quartz or feldspar pebbles in various quantities and without any coordination (Barabás & Barabás-Stuhl 1998). Practically, 100% of the pebbles of the older beds are volcanic rock fragments: rhyolite, rhyodacite and its pyroclastics and "melarhyolite" (i.e., subvolcanic or dyke rock with rhyolitic composition and microgranophyric texture). Moving upwards in the sequence, metamorphic rock fragments occur in progressively larger quantities. The K-feldspar and plagioclase content is significant, but the sodium-content of the rock is low due to the intensive decay of the plagioclases. The potassium-content of the rock is high due to the high muscovite-content (Fazekas 1987). The cementation can be silica, sericite, hematite and carbonate, in the drilling cores anhydrite is significant, too (Bodor & Szakmány 2009;Varga 2009).
The Upper Permian Boda Claystone Formation (formerly Boda Siltstone Formation) crops out on a larger surface, with a maximum of 1000 m thickness. This formation consists of the alternation of predominantly red, reddish brown, albite-containing siltstone and claystone. At the lower part, it contains greenish grey sandstone, sandy siltstone and claystone intercalations (Varga et al. 2006). The major rock types of the formation are claystone, siltstone, sandstone, albitolite and dolomite. There are many transitional types, too. The sandstone bands are usually intercalations within the very fine-grained bands (Árkai et al. 2000;Barabás & Barabás-Stuhl 1998;Máthé 1998;Varga et al. 2005;Varga et al. 2006). In its bulk rock chemical composition, the high sodium-content (5-8% Na2O) is characteristic (Árkai et al. 2000;Fazekas 1987;Máthé 1998).
The sandstone intercalations are usually red coloured with a shade of brown, grey or green, with a varying grain-size from fine-to coarse-grained. Parallel and cross-bedding occurs. These intercalations infrequently contain carbonized plant fossils and grey siltstoneclaystone-pebbles. The clastic grains are usually angular or only slightly subangular. The quantity of the cementation varies. In the medium-and coarse-grained sandstones the cementation is predominantly carbonatic, but in subordinate quantities hematite, illite or sericite, chlorite, albite and silica also occur. Carbonate veins are frequent (Varga et al. 2006). The sandstones contain 25-40% feldspars (more plagioclases, less K-feldspars), 20-30% quartz (monocrystalline and polycrystalline quartz), volcanic rock fragments (predominantly grains of recrystallized acidic volcanic groundmass and glass, together with neutral and basic volcanic rock grains) in large quantities, and a few detrital micas (muscovite and chloritized biotite). Metamorphic and sedimentary rock fragments (i.e., resedimented intraformational red siltstone and claystone grains) also occur. Accessory minerals (mostly in the fine-grained sandstones) are magnetite, ilmenite, zircon, monacite, rutile, apatite, tourmaline, titanite, and Cr-spinel (Varga et al. 2006).
The Upper Permian -Lower Triassic Kővágószőlős Sandstone Formation crops out in a larger surface than the Cserdi or Boda Formations with 150 to 1400 m total thickness. This formation is a fluvial sequence, with the rhythmical alternation of various coloured conglomerate, arkose sandstone, siltstone and claystone bands, with a significant refinement and then a coarsening in the grain size upwards in the sequence (Barabás & Barabás-Stuhl 1998).
In the beginning of the sedimentation of this formation, large quantities of granitemigmatite-originated clastic fragments (i.e., quartz, K-feldspar and quartz-K-feldspar intergrowths) occur (and the proportion of the metamorphic and volcanic rock fragments decreases). Upwards in the sandstones the amount of quartz is increasing (Fazekas 1987).
Based on the colour, petrographic and sedimentary characteristics, this formation was divided into four members.
The sandstones of The Bakonya Sandstone Member ("variegated sequence", Császár 1997) are poorly sorted, mainly red (or green, grey, variegated), dominantly coarse-grained sandstones (with significant amounts of fine-grained bands). The fine-grained sediments are granularly disintegrating (poorly consolidated, falling apart to pieces) and contain carbonate concretions.
The Kővágótöttös Sandstone Member ("grey sequence" Császár 1997) only rarely contains red and green bands, with varying grain-sizes (from conglomerates to silty claystones). This member is rich in organic material.
The Cserkút Sandstone Member ("overlying red sandstone" Császár 1997) consists of purplish red or red, dominantly medium-grained sandstones with sporadically occurring pebbles. Conglomerate, fine-grained sandstone and siltstone bands also occur. On the top of this member there is a few meters thick, reddish brown coloured sandstone band with carbonate concretions. This reddish brown sandstone is discoloured at some places.
At the transition part of the Kővágótöttös and Cserkút Members, a uranium ore-bearing "green sandstone bed" was formed.
The sandstones of the Tótvár Sandstone Member ("sandstone with violet gravel" Császár 1997) are crimson, purplish red or light purple coloured, unsorted, coarse-grained sandstones, with frequent pebbles and a silty matrix. The characteristic purple colour is the result of the large amount of rhyolite pebbles and angular rhyolitic rock fragments (Barabás & Barabás-Stuhl 1998).
The Jakabhegy Sandstone Formation has the widest distribution on the surface of all the Permian -Lower Triassic clastic sequences in the Western Mecsek mountains. This formation has a thickness between 60 and 380 m. The beds of the formation mainly crop out at the Jakab-hill. The transition between the Kővágószőlős and Jakabhegy Formations is continuous (Fazekas 1987).
Upwards in the sequence the amount of quartz is rising progressively in the sandstones. In the lower parts of the Jakabhegy Formation, plagioclase is totally missing, while the sodium-content of the rock is decreasing significantly compared to the lower members of the Kővágószőlős Formation. The amount of the potassium-feldspars is more or less the same in the whole sequence, but quartz-K-feldspar intergrowths are almost missing in the Jakabhegy Formation. Among the volcanic rock fragments, mostly various kinds of silicified rhyolite and tuffs are present, but rhyolite-fragments, which originate from the Gyűrűfű Rhyolite Formation, also occur as in the above-mentioned older formations. The most mature sandstone is the so-called "sandstone with orientated pebbles", which is a cross-bedded, palered or pale-violet sandstone, appearing in the upper part of the Jakabhegy Formation. Upwards the grain-size decreases and plagioclase-fragments and biotite reappear. The amount of the volcanic-fragments increases as well (Fazekas 1987).
In the whole Jakabhegy Formation the clastic constituents have the same characteristics: the predominant constituent is quartz, and in subordinate amount felsitic rhyolitic groundmass-fragments and K-feldspars are present. Quartz-feldspar intergrowths are very rare. Acidic plagioclase-fragments occur only in small amounts in the western territories of the formation, only in the upper part of the sequence. The less mature beds of the sandstones are micaceous (mainly muscovite, rarely biotite; Fazekas 1989).

Distribution of the framework grains (quartz-feldspar-rock fragments)comparison
Beside the average distribution-data of the artefacts, Figure 13 shows the representative distribution-data of the Balatonfelvidék Sandstone Formation (matured and unmatured sandstone types, Csernussi 1984;Fülöp 1990;Majoros 1998), as well as the average distribution-data of the Permian -Lower Triassic age sandstones form the Western Mecsek mountains (Fazekas 1987;1989). Data on the precise distribution of the Boda Formation are currently missing.
Subgroup I/1 and I/2 of the archaeological finds are lithic arenites (litharenites) and sublitharenites. Their composition lies in the field of the matured variant of the Balatonfelvidék Sandstone Formation.
Group II has a transitional composition between subarkoses and sublitharenites very near to the average composition of the Jakabhegy Sandstone Formation.
The other formations of the Mecsek mountains display a higher feldspar-and rockfragment-content and less quartz.

Bulk rock chemistry -comparison
The major-, trace-and RE-element patterns of the finds (see Table 1) have been compared with the data of all the above mentioned formations (Balaton-Highland: data of recently gathered red sandstone samples (Tables 2-4, sampling locations see Figure 12) and data from Csernussi 1984; Western Mecsek mountains: data of the sandstones and siltstones from drilling cores from Varga (2009) (Figures 14-25).

Major element patterns -comparison
The major element patterns of the comparative samples of the Balatonfelvidék Sandstone Formation (Figure 14) -similarly to the artefacts -show less sodium-, calcium-and magnesium-content than the values of the Upper Continental Crust (UCC) by Taylor & McLennan (1985) and McLennan (2001), with the exception of one older data-set from Csernussi (1984). They show a slightly higher silica-content. They have various iron-, alumina-, titanium-, potassium-and manganese-contents. The major element composition of Group I artefacts fits well within the composition range of the Balatonfelvidék Sandstone Formation. Group II artefacts have a bit differing composition: lower titanium-, higher potassium and sodium-content.
The sodium-and magnesium-content of the formations of the Western Mecsek mountains (Figures 15-21) are significantly higher than in the measured artefacts, with the exception of the Jakabhegy Sandstone Formation (and one sample of the Korpád Sandstone Formation). Nevertheless, the Korpád Sandstone Formation can be excluded from the possible sources because of the composition and distribution of the clastic grains. The potassium-content of the Mecsek samples is near to the potassium-content of Group II artefacts, i.e., significantly higher than the potassium-content of Group I. So, the major element composition of Group II artefacts fits most within the composition range of the Jakabhegy Sandstone Formation.

Minor and REE patterns -comparison
The minor element patterns of the sandstones and siltstones of the Balatonfelvidék and the Jakabhegy Formation are various within both formations, nevertheless the minor element patterns of Group I artefacts fits better with the patterns of the Balatonfelvidék Formation (Figure 22), while the patterns of Group II artefacts fits more with the Jakabhegy Formation ( Figure 23). In the second case the fitting is not as good as in the case of Group I. (2020)    The rare earth element content of the sandstones of the Balatonfelvidék Formation ( Figure 24) has greater variability than the REE-content of the sandstones and siltstones of the Jakabhegy Formation (Figure 25). The REE patterns of Subgroup I/1 of the artefacts fits better to the patterns of the Balatonfelvidék Formation, while the patterns of Group II artefacts fits better to the Jakabhegy Formation. The REE patterns of Subgroup I/2 of the artefacts (the discoloured ones) lie between the other groups (Compare Figures 24-25). (2020)

Discussion and conclusions
Based on the results of the above investigations and the comparative data of the possible source rocks the most probable origin of the raw material of the artefacts can be selected.
The red sandstones of the Western Mecsek mountains -except the Jakabhegy Sandstone Formation -can be excluded from the possible sources, primarily because of the high potassium-feldspar content, and because of their sodium-and magnesium-content, which is significantly higher than the sodium-and magnesium-content of the artefacts.
Other disqualifying petrographic characteristics of the following Formations from the Western Mecsek mountains are: The Korpád Sandstone Formation can be excluded from the possible sources because the amount of the rock-fragments within the framework grains is much higher than in the artefacts (see Figure 13), and among these rock fragments is a unique andesitic rock fragment type (with a characteristic appearance). This rock fragment type is not present in the raw material of the artefacts.
The Cserdi Formation can be excluded because of the amount of the rock-fragments within the framework grains, which is much higher than in the artefacts (see Figure 13), the high plagioclase content, the poor sorting of the rocks and the much larger amount of matrix compared to the raw material of the artefacts.
The Bakonya Sandstone Member of the Kővágószőlős Sandstone Formation can be excluded because of the poor sorting of the rocks and the poor consolidation of the finegrained sediments -these types are granularly disintegrating (falling apart to pieces), and therefore not useful as raw material.
The Kővágótöttös Sandstone Member of the Kővágószőlős Sandstone Formation can be excluded because of the high amount of organic material, which is not present in the artefacts analysed so far.
The Cserkút Sandstone Member of the Kővágószőlős Sandstone Formation can be excluded because of the amount of feldspars, which is too large in comparison to the artefacts.
The Tótvár Sandstone Member of the Kővágószőlős Sandstone Formation can be excluded because of the poor sorting of the rocks and the number of rhyolite-fragments, which is too large in comparison to the artefacts.
The artefacts of Group I are very similar -in the appearance of the respective components and the proportion of the framework grains (see Figure 13) and in its chemical composition (see Figure 14) -to the sandstones of the Red Sandstone and Siltstone Member of the Balatonfelvidék Sandstone Formation, and here primarily to the second facies type. This type is a mature sandstone, almost void of feldspar (litharenite), in which quartz and rock fragments are predominant among the clastic grains. This facies type is characteristic of the confines of the Southern Balaton Highland and the lower part of the Balatonfelvidék Sandstone Formation in the Northern Balaton Highland (see Figure 12).
The artefacts of Group II are very similar -in the appearance of the respective components and the proportion of the framework grains (see Figure 13), as well as in its chemical composition (see Figure 21) -to the red sandstones of the Jakabhegy Sandstone Formation, especially to the higher levels of the formation, where the number of volcanic rock fragments and micas increase and plagioclase is sporadically present (see Figure 12).
The distribution of the red sandstone raw materials corresponds well to the trend that the people of the Balatonőszöd -Temetői dűlő site made their tools mainly from local raw materials, e.g., basalt and basaltic lapilli tuff from the Balaton-Highland (Péterdi 2011;Péterdi et al. 2011;2014a). The raw material of some tools, however, originates from regional sources (from a distance of more than 30 km), e.g., from alkaline basic rocks ("trachydolerites") and a white, andalusite-bearing two-mica granite from the Mecsek mountains (Péterdi 2011). On the site, only a few polished stone artefacts were found made of raw material from distant sources (more than 200 km), e.g., from nephrite and serpentinite from Lower Silesia (Poland), and a contact metabasite from the Krkonoše-Jizera Crystalline Unit (Czech Republic;Péterdi 2011;Péterdi et al. 2014b). (2020)