GC_2-2013_KB.indd 1. INTRODUCTION Much of the sedimentary fi ll of the Neogene Pannonian Ba- sin System was deposited in the Late Miocene – Early Plio- cene Lake Pannon, a large, long-lived, brackish lake popu- lated by a highly endemic “Ponto-Caspian-type” biota. In particular, cardiid bivalves refl ect the extraordinary diversity with more than 200 species in the lake (MÜLLER et al., 1999; GEARY et al., 2000). Whereas high diversity in some other groups, such as the gastropods, was achieved by a combined effect of in situ evolution and inheritance from Early – Middle Miocene lakes (HARZHAUSER & MAN- DIC, 2008), Lake Pannon cardiids probably all originated from ancestors living in the restricted marine environment of the Middle Miocene Sarmatian sea (e.g. VRSALJKO, 1999). Historically, the fi rst signifi cant endemic cockle as- semblage from the lake was described by HÖRNES (1862) from the village of Árpád (today part of Pécs), southern Hun- gary. Later these cardiids played an outstanding role in the classifi cation of Miocene and Pliocene brackish cockles of the entire Paratethyan region. Although similar faunas are well-known from the southern regions of the Pannonian Ba- sin, especially in Croatia (e.g. BRUSINA, 1884; BASCH, 1990), some of the Árpád species are very rare elsewhere. For example, the type species of the genus Lymnocardium, L. haueri, has not been known to occur in any other locality (reports on L. haueri from Serbia (STEVANOVIC, 1951) and Croatia (BASCH, 1990) refer to a morphologically clearly distinct form, probably another species). AB STRA CT A classic but very rare “Árpád-type”mollusc assemblage, representing the endemic fauna of the Late Miocene–Early Pliocene Lake Pannon, was discovered in Kozármisleny (near Pécs, southern Hungary). The fossils were collected from silt layers deposited in the shallow sublittoral zone of Lake Pannon, exposed in an 8–10 m high road cut. The assemblage contained some very rare species, including the type species of the genus Lymnocardium, L. haueri (M. HÖRNES). Palynological investigations from the same layers failed to yield age-diagnostic dinofl agellates, and pointed to a brackish – freshwater depositional environment and warm temperate climate. Keywords: Pannonian Basin, Lake Pannon, molluscs, palynomorphs, granulometry  Geologia CroaticaGeologia Croatica A new occurrence of a classic “Árpád-type” mollusc fauna from the Upper Miocene of Kozármisleny, southern Hungary  Lajos Tamás Katona1, János Kovács2, Imre Magyar3, Mária Sütő-Szentai4 and Tibor Berta5 1 Natural History Museum of Bakony Mountains, H-8420 Zirc, Rákóczi tér 3-5. Hungary; (fi nci99@freemail.hu) 2 Department of Geology, University of Pécs, H-7624 Pécs, Ifjúság str. 6, Hungary; Environmental Analytical & Geoanalytical Research Group, Szentágothai Research Centre, University of Pécs, H-7624 Pécs, Ifjúság str. 20, Hungary; (jones@gamma.ttk.pte.hu) 3 Research Group for Paleontology, Hungarian Academy of Sciences-Hungarian Natural History Museum- Eötvös University, POB 137, H-1431 Budapest, Hungary; (immagyar@mol.hu) 4 H-7300 Komló, Május 1. u. 7, Hungary; (szentai.maria@gmail.com) 5 H-8200 Veszprém, Sólyi u. 2, Hungary doi: 10.4154/gc.2013.08 Geologia Croatica 66/2 111–118 5 Figs. Zagreb 2013 Geologia Croatica 66/2Geologia Croatica 112 The original descriptions by HÖRNES (1862) were based on donated specimens, and the exact locality where the shells had been collected remained unknown. Recently SZÓNOKY et al., (1999) measured a fossiliferous outcrop located immediately south of Árpád. Some 2.5 km NE of their locality, in the area of the village of Kozármisleny, a road cut was deepened in 2008 as part of the construction of the M6 highway system, exposing fossiliferous silt layers deposited in Lake Pannon. When visiting the outcrop, we were allowed only a restricted time for scanning the sequence and collecting samples. The mollusc fauna of the outcrop, however, proved to be very remarkable. The 10 bivalve (in- cluding 8 cardiid) and 4 gastropod species correspond to the classic Árpád fauna, containing the same morphological types and including some of the rarities (L. haueri, L. hun- garicum, L. arpadense, Pteradacna pterophora). This paper gives a brief account of the outcrop and its mollusc fauna, complete with the results of palynological investigations. 2. THE KOZÁRMISLENY OUTCROP The excavation site (46°05’N and 18°27’E) is located in the Pécs Basin, between the villages of Kozármisleny and Árpád (Nagyárpád, today part of Pécs) in southern Hungary (Fig. 1), at an elevation of 160 m above sea level. The Pécs Basin is fi lled with lacustrine, fl uvio-lacustrine, and aeolian depos- its of Miocene to Pleistocene age. In the southern margin of the basin, the layers dip approximately 1–3° to the south- southeast (SEBE et al., 2008). The north to south oriented road cut exposed the depos- its of Lake Pannon in an 8–10 m thick sequence below a thin Pleistocene loess cover. The section is composed primarily of yellowish-gray, medium- to coarse-grained silt, with 20–30 cm thick intercalations of fi ne-grained silt. Layers of both the eastern (A) and western (B) walls were numbered from bottom to top. Layers of wall A (Fig. 2) were continuously sampled at 10–20 cm intervals for laser diffraction grain-size analysis (Fritsch Analysette 22), following the approach of KONERT & VANDENBERGHE (1997) and KOVÁCS (2008). The gray-coloured, fi ne silt layers were laminated. Between the lamina, magnesium-oxide fi lms occurred. The yellowish- gray, medium- to coarse-grained silt layers showed cross to wavy lamination. The medium- and fi ne-grained silts were very poorly-sorted, strongly positively skewed, and ex- tremely leptokurtic (Fig. 2, A2, 3, 5, 7, 9). Their grain-size frequency curves were unimodal (Fig. 3.). The coarse silts were also very poorly-sorted, strongly positively skewed, and extremely leptokurtic, but the grain-size frequency dis- tributions tended to exhibit a weakly-developed bimodality (Fig. 2., A1, 4, 6, 8, 10 and Fig. 3.). The grain size parame- ters and the bimodality of the central parts of the frequency distributions (Fig. 3.) indicate a shallow sublittoral deposi- tional environment with occasionally signifi cant effects of wave action, characteristic of both marine (GOLDBERY, 1980; TAMURA, 2004; BARUSSEAU, 2011) and lacustrine (XIAO et al., 2012) environments. Most of the layers seemed to be barren of molluscan fos- sils or contained only shell fragments, but silt layers A1 to A3 and a very-fi ne, yellow sand layer at the bottom of wall B (B1) contained abundant and well-preserved shells. Figure 1: Geographic position of the Kozármisleny profi le. Katona et al.: A new occurrence of a classic "Árpád-type" mollusc fauna from the Upper Miocene of Kozármisleny, southern Hungary Geologia Croatica 113 3. MOLLUSCS Apart from the fossiliferous layers A1 to A3 and B1, mol- lusc shells were also collected from debris at the foot of the walls. The following forms were identifi ed: Congeria rhomboidea rhomboidea HÖRNES, 1862 (Fig. 4d). Well-preserved specimens, 5–7 cm in length and 4–5 cm wide, occurred in layers A1 to A3. Several dozen specimens were collected, some with articulated valves, some as single valves. Dreissenomya unionides FUCHS, 1870 (Fig. 4h). A sin- gle specimen was discovered, 4 cm long and 2.5 cm wide. Lymnocardium arpadense (HÖRNES, 1862) (Fig. 4j). A mass occurrence of single and articulated valves, ca. 3 cm in length and 2 cm in width, occurred in layer B1. Lymnocardium haueri (HÖRNES, 1862) (Fig. 4i). 3 specimens (length 4–4.5 cm, width 4 cm) were collected from layer B1. Lymnocardium hungaricum (HÖRNES, 1862) (Fig. 4e). Three almost intact specimens and several broken ones and fragments were observed, mostly in layer A3. The valves are 7–9 cm long and 6–7 cm wide. Lymnocardium majeri (HÖRNES, 1862) (Fig. 4k). A large number of excellently preserved specimens were col- lected from layers A2 and B1, with an average size of 3 cm length and 2.5 cm width. Lymnocardium rogenhoferi (BRUSINA, 1884) (Fig. 4m). Four specimens, all belonging to the Árpád morpho- type, were recovered from layer A2. None of the valves ex- ceeded 2 cm in length. Lymnocardium schmidti (HÖRNES, 1862) (Fig. 4f). Three specimens, 3–7 cm in length and 3–6 cm in width, were discovered in layer A3. Caladacna steindachneri (BRUSINA, 1884) (Fig. 4n). Two internal moulds (steinkern) were collected from layer A2. Pteradacna pterophora (BRUSINA, 1884) (Fig. 4g). Three partial specimens were collected from debris. Radix kobelti (BRUSINA, 1884) (Fig. 4a). One speci- men was observed in layer A1. Radix lytostomopsis (BRUSINA, 1902) (Fig. 4b). One specimen occurred in layer A1. Zagrabica cyclostomopsis BRUSINA, 1884 (Fig. 4c). 3 specimens were discovered, with an average size of 0.9 cm height and 0.6 cm width, in layer A1. Figure 2: The Kozármisleny road cut (wall A) with grain-size distribution curves of the Upper Miocene layers. Figure 3: Grain-size spectra of samples from diff erent layers in wall A. Geologia Croatica 66/2Geologia Croatica 114 Figure 4: Molluscs from the Kozármisleny profi le. a: Radix kobelti, b: Radix lytostomopsis, c: Zagrabica cyclostomopsis, d: Congeria rhomboidea rhom- boidea, e: Lymnocardium hungaricum, f: Lymnocardium schmidti, g: Pteradacna pterophora, h: Dreissenomya unionides, i: Lymnocardium haueri, j: Lym- nocardium arpadense, k: Lymnocardium majeri, l: Valenciennius reussi, m: Lymnocardium rogenhoferi, n: Caladacna steindachneri. Scale bar: 2 cm for a–c, 1 cm for d–n. Katona et al.: A new occurrence of a classic "Árpád-type" mollusc fauna from the Upper Miocene of Kozármisleny, southern Hungary Geologia Croatica 115 Valenciennius reussi (NEUMAYR, 1875) (Fig. 4l). Two specimens were collected from layer A1. 4. PALYNOLOGICAL INVESTIGATIONS Three samples from layer A1 were collected for palynolog- ical analysis. The objective was to better assess the biodiver- sity in this environment, and to provide data for biostrati- graphic and environmental interpretation. Palynological samples were prepared using standard processing techniques at the Laboratory of the Hungarian Geological Institute. The samples were treated with HCl (36%) and HF (40%) to remove the mineral fraction, and a heavy liquid (ZnCl2, density 2.2 g/cm3) was used to separate the organic matter from the undissolved inorganic compo- nents. The organic residue was not sieved, and additional oxidation was unnecessary. Organic residue was mounted in glycerine jelly and three slides were investigated. Two dino- cyst taxa, three fresh water algae and 18 sporomorph taxa were identifi ed. 4.1. Dinofl agellates The dinofl agellate assemblage consisted of two forms: cf. Batiacasphaera sp. DRUGG 1970, 12 specimens (Fig. 5, 4), and Gonyaulacaceae sp. indet. LINDEMANN 1928, only one specimen (Fig. 5, 7). The Batiacasphaera-like dinocyst of layer A1 is poorly preserved. It is similar to those forms that occur elsewhere in the Galeacysta etrusca Zone, (younger than 8 Ma) in hav- ing an intercalary archeopyle and punctated ornamentation, but differs from them in its habit and glassy appearance. Go- nyaulacaceae sp. indet. is well-preserved. A reworked origin for this specimen can be excluded. It resembles some well- known dinofl agellates from the Galeacysta etrusca Zone (Gonyaulax spinifera – G. digitalis), but its tabulation is not identical with them. Neither form is suitable for a more precise biostrati- graphic evaluation. Their presence indicates a probable brackish environment. 4.2. Chlorophyta The samples contained Botryococcus braunii KÜTZING 1849, a green alga common in both brackish and freshwater ecosystems worldwide. Mougeotia laetevirens (A. Braun) WITTROCK 1877 and a freshwater Spirogyra sp. indicate the presence or proximity of a freshwater environment. 4.3. Sporomorphs The following forms were identifi ed: Abiespollenites latisaccatus (TREVISAN 1967) KRU- TZSCH 1971 (Fig.5, 6) Abiespollenites maximus (KRUTZSCH 1971) NAGY, 1985 Abiespollenites sivaki NAGY, 1985 (Fig.5, 8) Abietinaepollenites microalatus (R. POTONIÉ, 1932) R. POTONIÉ, 1951 Alnipollenites verus R. POTONIÉ, 1934 Betulaepollenites betuloides (PFLUG, 1953) NAGY, 1969 Cedripites crassiundulicristatus (TREVISAN, 1967) KRUTZSCH, 1971 (Fig.5, 1–3) Cedripites dacrydioides KRUTZSCH, 1971 Chenopodipollenites multiplex (WEYLAND & PFLUG, 1957) KRUTZSCH, 1960 Ericipites callidus (R. POTONIÉ, 1931) KRUTZSCH, 1970 Hydrosporis levis KRUTZSCH, 1962 Nymphaeaepollenites pannonicus NAGY, 1969 Piceapollenites neogenicus (NAGY, 1969) KRU- TZSCH, 1971 Pinuspollenites labdacus (R. POTONIÉ, 1932) R. PO- TONIÉ, 1958 Plantaginacearumpollenites miocaenicus NAGY, 1963 Polypodiisporites favus (R. POTONIÉ, 1931) R. PO- TONIÉ, 1933 Tsugaepollenites verrucatus (KRUTZSCH, 1971) NAGY, 1985 (Fig. 5, 5) Ulmipollenites undulosus WOLFF, 1934 The coniferous species with abundant fi r (Abiespol- lenites), pine (Pinuspollenites), cedar (Cedripites) and less spruce (Piceapollenites) refl ect the composition of a distant mountainous vegetation. The broad-leaved forms are repre- sented by birch (Betulapollenites) and elm (Ulmipollenites), the ferns are represented by Polypodiisporites and Laevigat- osporites. Alder (Alnipollenites) probably occurred at the lake shore and in marshes. Grasses barely appeared in the samples. The aquatic vegetation is represented by fl oating ferns (Hydro sporis) and water lilies (Nymphaeaepollenites). This pollen spectrum can be readily compared to those of other Late Miocene and Early Pliocene samples from the Transdanubian region of Hungary, such as those in drill cores from Lake Balaton (NAGY-BODOR, 1988) and from the borehole Pula-3 (NAGY, 2005), respectively. In spite of all the similarities, the Kozármisleny samples contain less broad- leaved species and fewer grasses than the two other spectra, and indicate a relatively humid, warm temperate climate. 5. DISCUSSION AND CONCLUSIONS As indicated by grain size and sedimentary structures, the silt layers of the Kozármisleny outcrop were deposited in the shallow sublittoral zone of Lake Pannon. The ecological de- mand of molluscs supports this interpretation. L. majeri, L. rogenhoferi, Pteradacna pterophora, and Valenciennius are known to have been sublittoral dwellers. L. arpadense, sim- ilarly to its ancestor L. diprosopum, however, usually occurs in littoral sands (GEARY et al., 2010). At the time of depo- sition, the lake shore was situated a couple of kilometres to the northwest, possibly in the Mecsek Mountains. Recently SEBE et al., (2013) described the occurrence of a wave-cut Geologia Croatica 66/2Geologia Croatica 116 platform, together with the mollusc Dreissenomya unioides, a burrowing dreissenid (also present in the Kozármisleny fauna), from the southern slope of the Mecsek Mountains, at 380 m above sea level. The diverse cardiid assemblage seems to indicate brack- ish water, whereas the algae and sporomorphs argue for a brackish to freshwater environment. Spores and pollen indi- cate a warm temperate climate. The palynological investigations failed to identify age- diagnostic dinofl agellates. The great similarity of the mol- lusc fauna to the classic Árpád one however, allows infer- ence of the Prosodacnomya vutskitsi Zone (7–5 Ma). Although the Árpád outcrop displays more sand layers, the close proximity and identical fauna suggests that the two outcrops, Árpád and Kozármisleny, expose the same sedi- mentary rock body. Figure 5: Pollen and algae from layer A1. 1–3: Cedripites crassiundulicristatus (TRE- VISAN, 1967) KRUTZSCH, 1971 (55–56 μm); 4: cf. Batiacasphaera sp. (DRUGG, 1970) (56 μm); 5: Tsugaepollenites verrucatus (KRUTZSCH, 1971) NAGY, 1985 (54 μm); 6: Abiespollenites latisaccatus (TREVISAN, 1967) KRUTZSCH, 1971 (133 μm); 7: Gonyau- la caceae sp. LINDEMANN, 1928 (46×39 μm); 8: Abiespollenites sivaki NAGY, 1985 (94 μm). Katona et al.: A new occurrence of a classic "Árpád-type" mollusc fauna from the Upper Miocene of Kozármisleny, southern Hungary Geologia Croatica 117 ACKNOWLEDGMENT The authors thank Krisztina SEBE, Viktória BARANYI, and two anon- ymous reviewers for their comments on the earlier version of the man- uscript. 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