 Geologia Croatica 65/3 299–322 26 Figs. Zagreb 2012 1. INTRODUCTION The Pennsylvanian was one of the most important times for coal formation in Earth history. The lowland areas of Eura­ merica and China were covered by extensive wetland forests dominated by arborescent lycopsids and tree ferns (OP LUŠ­ TIL & CLEAL, 2007). Extensive floras are known from Up­ per Silesia, the Intra Sudetic Basin, Central and Western Bo­ hemia, South Wales and from the Pennines (for more details see OPLUŠTIL & CLEAL, 2007). In Italy (Southern Alps, Tuscany, Sardinia, Liguria), se­ veral outcrops of terrestrial sediments have also yielded Pennsylvanian floras. Although the Carboniferous sections are mostly scattered and of limited extent, these Pennsylva­ nian occurrences are fundamental for regional correlations and palaeogeographic reconstructions. Therefore the goal of this paper is to provide an updated review on the main sections which have yielded rich Penn­ sylvanian plant megafossils and palynofloras, hoping that a future taxonomic revision of them can provide a better pic­ ture of the Pennsylvanian floras of Italy. 2. THE MAJOR PENNSYLVANIAN FLORAS IN ITALY From Northern to Southern Italy, the most important out­ crops are mainly concentrated in four different regions (Fig. Ab STRA CT The paper provides an overview of the main Pennsylvanian sites in Italy yielding associations rich in plants and/or palynomorphs. So far in Italy, the principal outcrops are located in the Southern Alps, Tuscany and Sardinia. In the Western Southern Alps and bordering Switzerland, Westphalian outcrops are small and scattered. Nevertheless, one of them yielded an abundant fossil flora, stored at the Museo Civico di Storia Naturale of Milan, (Venzo and Maglia Collection). In the Carnic Alps, (Eastern Southern Alps), continental deposits of Moscovian to Gzhelian age also oc­ cur near the border with Austria. They have produced a high number of preserved plant fossils, presently stored in the Museo Friulano di Storia Naturale of Udine. In Tuscany, the two main sections yielding Westphalian to Autunian floras are those of the Iano and Pisani Mountains. A rich collection of plant fossils from those sites is hosted at the Museo di Storia Naturale of Florence University and at the Museum of Natural History of Pisa University. In Sar­ dinia, plant fossil sites are located in the south west and central east parts of the island. The San Giorgio Basin (Igle­ siente subregion) and the Tuppa Niedda section (Arburese subregion) are late Westphalian – early Stephanian in age. In the Barbagia at Seui­Seulo and the Gerrei subregions, other continental basins yielded transitional “Stephanian­ Autunian” fossil plant associations. The slabs are stored as part of the Lovisato Collection at the Lovisato Museum of the Chemical and Geoscience Department of Cagliari University. Smaller historical outcrops of Carboniferous age are also known from other Italian regions, such as Liguria. Keywords: Pennsylvanian, Southern Alps, Tuscany, Sardinia, plant fossils, palynomorphs, fossil plant collections Geologia CroaticaGeologia Croatica Pennsylvanian floras from Italy: an overview of the main sites and historical collections  Ausonio Ronchi1, Evelyn Kustatscher2, Paola Pittau3 and Giuseppe Santi1 1Dipartimento di Scienze della Terra e dell’Ambiente, Università di Pavia; (ausonio.ronchi@unipv.it; gsanti@unipv.it) 2Museo di Scienze Naturali dell’Alto Adige, Bolzano; (evelyn.kustatscher@naturmuseum.it) 3Dipartimento di Scienze Chimiche e Geologiche, Università degli Studi di Cagliari, Italy; (pittaup@unica.it) doi: 104154/gc.2012.20 Geologia Croatica 65/3Geologia Croatica 300 1), excluding small and debated outcrops in Western Ligu­ ria. They are briefly described in paragraph 5 and synthe­ sized here below. 2.1. Southern Alps 2.1.1. Western Southern Alps/Canton Ticino (Switzerland) Sparse continental Pennsylvanian successions crop out in the western Southern Alps, especially in the so­called Vare­ sotto­Lugano area, to the West of Lake Como (Fig. 2). The main localities are Alpe Logone, Val Rezzo, Mesenzana, Grantola, Bèdero, Bosco Valtravaglia­Fabiasco, Val Tresa on the Italian side of the border and Manno (and other small sections in Val Colla, Cadro, Denti della Vecchia, etc.) in the Canton Ticino area (Switzerland). The successions, called by many authors the “Basal Con­ glomerate”, are alternations of conglomerates, sandstones and siltstones composed of metamorphic and vein­type quartz clastics. These units were also name “non­porphyric” conglo­ merates (e.g., BAGGIO & DE MARCO, 1960), in order to distinguish them from younger deposits where volcano­clastic deposits occur. The bedding of these generally coarse­grained sediments is often irregular and some crude channelling is ob­ served. Deposits occur generally pinched along major tectonic lines or in stratigraphic non­conformities above the metamor­ phic basement, and represent the “Southern Alps sedimentary front”. These sediments are the product of the erosion of the Variscan mountain chain, and the contact with the crystalline Figure 1: Location of the main Pennsylvanian sites in Italy. 1 – Western Lombardy region and Canton Ticino (Switzerland); 2 – Carnic Alps (Alto Adige and Tyrol, Austria); 3 – Tuscany (Pisani Mountains and Iano); 4 – South western, central and South eastern Sardinia. Figure 2: Location of the main outcrops of Pennsylvanian sections in the Western Southern Alps and Canton Ticino (from PITTAU et al., 2008a, mod.) A – Italian/Swiss sector between Lake Maggiore and Lake Lugano; B – Italian/Swiss sector between Lake Lugano and Lake Como. Bold line is the Italian- Swiss border. Ronchi et al.: Pennsylvanian floras from Italy: an overview of the main sites and historical collections Geologia Croatica 301 basement is marked by a gap of unknown time (BERTOTTI, 1991). The thickness varies from 0–15 m in the Val Sanagra (VENzO & MAGLIA, 1947), to 20–30 m in the Val Rezzo (Fig. 3) and in the upper Val Colla, and to about 100 m beneath the Denti della Vecchia (LEHNER, 1952). The finer grey­to­reddish clastic sediments structurally de­ veloped in a basin situated south of the Marzio Lineament, (or Brusimpiano­Cabiaglio Lineament). They generically follow the initial deposition of volcanic­rich conglomerate, and are called the Mesenzana Formation (CASATI, 1978; see Fig. 5). The age of all the Upper Palaeozoic, strongly tectoni­ cally stressed, sedimentary successions, scattered over a wide area between Lake Como, Lake Maggiore and Ticino, has long been debated as being between the Westphalian and Stephanian (e.g. LEHNER, 1952; VENzO & MAGLIA, 1947; STADLER et al., 1976; CASATI, 1978; GAETANI et al., 1986). The whole region, where all these so­called “Basal Con­ glomerats” crop out, can be subdivided into two sectors (Fig. 2) which, from E to W, are described below. Figure 3: Lithological and stratigraphic section South-East of Cimadera-Val Rezzo (from LEHNER, 1952, mod.). The Upper Carboniferous (i.e. Pennsylvanian) conglomerates and the overlying “Verrucano-Servino Series” are tectonically separated by a thinband and of “Gneiss chiari”. 1– dolostones, 2– micaceous, clayey sandstones, 3 – mainly quartzose sandstones, 4 – arkosic sandstones, 5 – conglomerate breccia, 6 – sandy dolostones and dolomitic sandstones, 7 – conglomerates, 8 – sandstones, 9 – coal bearing-sandstone, 10 – “Gneiss chiari”, 11 – phyllonites. Geologia Croatica 65/3Geologia Croatica 302 SECTOR B To the East, between the Lugano and Como lakes, some small outcrops with fine to coarse grained clastic deposits occur (Fig. 2B), including Alpe Logone, which has yielded a rich macrofloral association. The first report on Carbonife­ rous macrofloras from this locality is from MAGNANI (1946), who discovered impressions and casts of Calamites, Sigillaria and Lepidodendron. In the mid 20th century, Silvio Venzo and Luigi Maglia (VENzO & MAGLIA, 1947; VENzO, 1951) collected more than 2000 leaf compressions and im­ pressions from the anthraciferous and silicified beds at Alpe Logone, (in the Val Sanagra and, particularly, in Val Ga rias ca). They described about 22 genera and 75 species belon ging to the Sphenophyllaceae (Sphenophyllum), Equisetales (e.g., Calamites, Asterophyllites, Annularia), Lycopodiales (e.g., Lepidodendron, Knorria, Lepidophyllum; Sigillaria­ ceae, Sigillaria, Stigmaria; Ulodendraceae), Cycadaceae, Cordaitales, Filicales and Pteridospermales (e.g., Pecopteris, Figure 4: Some examples of Plant fossils from the Pennsylvanian of the Alpe Logone/Val Sanagra (W Lombardy), from Venzo Collection hosted in Milano Museum (determinations by S. Opluštil and J. Pšenička). A. Pecopteris (Lobatopteris) cf. simoni (sample B1519); B. Linopteris obliqua (sample B1605); C. Paripteris linguaefolia (sample B1895); D. Annularia radiata (sample B1888); E. Bothrodendron sp. (sample B1686); F. Sigillaria rugosa (sample B1722); G. Alepthopteris cf. grandinioides var. grandinioides (sample B1902b). Ronchi et al.: Pennsylvanian floras from Italy: an overview of the main sites and historical collections Geologia Croatica 303 Mariopteris, Neuropteris, Linopteris). Poorly preserved banded fragments of Sigillaria were also reported from the arenaceous layers. The rich collection, housed in the Museo Civico di Storia Naturale of Milan, is currently under revi­ sion (Fig. 4). The flora was ascribed to the late Westphalian (Westpha­ lian C) by VENzO & MAGLIA (1947) and VENzO (1951). These authors consider the flora of the Alpe Logone to be slightly older than the flora from the Manno Conglomerate in Ticino (see below), even if both show close affinities. Accor­ ding to PITTAU et al. (2008a), the very rich Logone and Man­ no’s macrofloristic assemblages allow assignment to the Bol­ sovian (Westphalian C) or to the Duckmantian­Bolsovian (Westphalian B–C) transition. SECTOR A To the West, between the Maggiore and Lugano lakes (Fig. 2A), several small outcrops of the Manno conglomerate are known. The type section crops out in the homonymous vil­ lage in Ticino (Switzerland). The fossiliferous successions are characterized by alternations of fine layered sandstones and conglomerates of light­grey colour. Locally they bear anthracite­type rock layers with poorly preserved plant re­ mains. As in Manno, these deposits occur in very scattered outcrops, generally pinched along tectonic lines. They rep­ resent the oldest sedimentary units in the Western Southern Alps. The Manno conglomerates likely filled a fault­bounded intracontinental basin characterized by fluviolacustrine and fluviopalustrine environments. These deposits represent the base of an initial tectono­sedimentary cycle developed mainly during the Early to Middle Permian throughout the Southern Alpine domain (e.g., GAETANI et al., 1986; CAS­ SINIS & PEROTTI, 2007). From the Manno type­locality, HEER (1876) listed Ca- lamites cisti, Sigillaria elongata and S. elegans. ESCHER (1911), confirmed Calamites cisti, and Sigillaria elonga , but Figure 5: A simplified geological map and section of the Western Southern Alps (from CASATI, 1978, mod). This area relates generally to Sector A shown in Fig. 2. Geologia Croatica 65/3Geologia Croatica 304 attributed the last species to S. tessellata. SORDELLI (1896), recognized 13 species; ten are common with the flora from the Alpe Logone, including five species of Sigillaria, and another five species among the genera Calamites, Lepido- dendron and Cordaites. He attributed the Manno flora to the early Stephanian, but with many Westphalian elements (SORDELLI, 1896). VENzO (1951) attributed the flora from Manno to the transition between the Westphalian B and Westphalian C, suggesting it to be slightly older than the flora from Alpe Logone (see above). JONGMANS (1950), related the floras of various Swiss localities (including Manno), first to the Westphalian B–C due to the presence of some elements such as Linopteris neuropteroides, cf. Pecop- teridium, Sigillariaephyllum, Cordaites cf. borassifolius, but later considered it to be slightly younger, most likely West­ phalian (“Mittleres Westphalen”, JONGMANS, 1960, p. 95). Along the Germignaga­Bèdero road on the eastern side of Lake Maggiore, some light grey coloured layers of sand­ stones and conglomerates also occur. Locally, they bear an­ thracite with badly preserved plant remains including Sigil- laria, which is putatively attributed to the Stephanian (VENzO & MAGLIA, 1947). Clasts of this succession show an origin from the metamorphic basement alone, but at the top of the Bèdero section, and in the very nearby outcrop, (i.e. along the Luino­Laveno railway­line), volcanic­rich conglomerates are also reported by these authors and thus suggesting a younger (Permian?) age for these latter sedi­ ments (Fig. 6). More recently, the Bèdero section (Lake Maggiore, Fig. 2A and Fig. 7) yielded a rich palynoflora, which allowed as­ signment of these sediments to the late Westphalian­early Stephanian (PITTAU et al., 2008a). In the sporomorphs, 42 genera and 76 species with one new genus (Cassinisporites) and ten new species have been distinguished. The Bèdero assemblages are suggested as being younger than the suc­ cessions studied from North­Eastern Italy, and to be more or less of the same age as the flora of San Giorgio (South­West­ ern Sardinia). The dominance of trilete spores, with a pro­ nounced taxonomic diversity, and Florinites pollen (over 70%), is indicative of a well­developed flora dominated by ferns, pteridosperms and Cordaitales, typical of a lowland flora (PITTAU et al., 2008a). 2.1.2. Eastern Southern Alps and border with Austria (Carnian Alps) The Carboniferous successions of the Eastern Southern Alps crop out in several localities of the Carnian Alps, near the border with Austria and in Carinthia (Fig. 8). They represent the lower part of the more than 200 metre­thick terrestrial­ transitional­marine Permo­Carboniferous sequence (Fig. 9). From the 1970’s onwards, Pennsylvanian plant mega­ fossils have been studied from several localities, mostly on the Austrian side, (e.g., VAN AMEROM et al., 1976; VAN AMEROM & SCHOENLAUB, 1992., FRITz, 1980, 1983; FRITz & BOERSMA, 1983; FRITz & KRA INER, 1993, 1994, 1995, 1997, 2006; VAN AMEROM & KABON, 2000). Nowadays, three different Permo­Carbo niferous basins are distinguished in the Carnian Alps, respectively around Forni Avoltri, Pramollo and Tarvisio (SELLI, 1963; VENTURINI, 1983, 1990a, b, 1991; VENTURINI et al., 1991). The Pra mollo Basin is the most important and extensive with several loca­ li ties (e.g., Passo Pramollo, Cason di Lanza, Monte Corona) yielding rich floras (Fig. 10). This basin has been studied in detail with respect to its sedimentology, stratigraphy, petro­ graphy and palaeomagnetics (e.g., VENTURINI, 1990a and ref. therein). The rich fossil content (brachiopods, crinoids, Zoophycos, fusulinids, plants; FRITz et al., 1990) has been used to constrain the age of the different formations and to Figure 6: Geological sketch sec- tions of the Pennsylvanian to La- di nian succession on the Germi- gnaga-Bèdero road and railroad, near Luino, Lake Maggiore (from VENZO, 1950, mod). Above: on the road to Bèdero; below: on the lakeside road and between the railway tunnels “Lunghi” and “Lavello”. 1. Basement mica- schists; 2. Pennsylvanian trans- gressive conglomerates and sandston es (Stephanian); 3. Reddish clayey sandstones (Per- mi an?-Scythian), 4. Reddish por- phyritic conglomera tes (late Scythian); 5. Dolostones (Ani- sian -Ladi nian); 6. Talus. Ronchi et al.: Pennsylvanian floras from Italy: an overview of the main sites and historical collections Geologia Croatica 305 reconstruct the evolution of the basin. The ichnoassemblages reflecting changes from terrestrial to lagoonal facies are also important (BAUCON & CAR VALHO, 2008). From base to top, the Pramollo Group (VENTURINI, 2002a, b), formerly the Auernig Group sensu SELLI (1963; see Fig. 9), is composed of the Meledis, Pizzul, Corona, Au­ ernig and Carnizza Formations. The Pramollo Group consists of cyclic, shallow­marine, clastic and carbonate deposits up to 1200 m thickness. Shore­face and offshore environments are quite common. Moreover, the regressive–transgressive cycles (“Auernig cyclothems”), in the upper part of this group have been related to eustatic sea­level changes due to the Permo­Carboniferous glaciation, where the carbonatic levels would correspond to interglacial phases with a sea­level rise covering this area (VENTURINI, 1990a, b; 1991; MASSARI et al., 1991). The most abundant flora comes from the Co­ rona Formation (A3 formation sensu VENTURINI, 1990a, b), a terrigenous succession of uppermost Gzhelian age, (Ma­ s sari et al. in VENTURINI et al., 2002b). Plant fossils are, however, widely distributed in most of the fine sandstones and pelites of the Bombaso Formation and basal Pramollo Group, (Meledis, Pizzul, basal Auernig and Car nizza Forma­ Figure 7: The Bèdero Section (from PITTAU et al., 2008a, mod). Geologia Croatica 65/3Geologia Croatica 306 tions, respectively A1, A2, A4 and A5 of VENTURINI 1990a, b, see Fig. 9). The Corona Formation is characterized by its almost complete lack of carbonatic levels (so far only one has been identified, see Krainer in VENTURINI, 1990b). It consists mainly of alternations of fine quartzose conglomerates, sand­ stones and siltstones corresponding to subaerial or paralic environments (VENTURINI, 1990a, b). There also exist, two transgressional acmes with fine siltstone, hummocky structures and a high abundance of marine fauna (brachio­ pods, crinoids, marine ichnofossils). Plant megafossils occur in the fine sandstones and pelitic levels (Fig. 10), and several sphenophyte trunks have been found in situ (with a diameter of up to 20 cm). Coal­rich levels of up to 30 cm have also been recorded from these horizons (SELLI, 1963). More than 2000 slabs with rich and well preserved plant remains from Casera Auernig, Casera Cordin Grande, Cason di Lanza, Creta di Lanza, Forca di Pizzul, Fontanone, La Scaletta, Mt. Auernig, Mt. Carnizza, Mt. Cocco, Mt. Corona, Mt. Pic Chiadin, Mt. Pizzul, Passo Pramollo, Passo Volaia, Pian di Lanza, Pontebba, Rio Bombaso, Rio Bruca, Rio dai Amplis, Rio degli Uccelli (Vogelbach) and Sella Barizze (Fig. 11), are currently stored at the Museo Friulano di Sto­ ria Naturale of Udine (Fig. 12; courtesy of Udine Museum), at the University of Innsbruck (Austria) and at the Landes­ museum Klagenfurt (Germany). The floras of the Austrian side of the border have been mostly studied since the 1980’s. Grouping the floras stratigra­ phically (Fig. 13), the following information can be given (for more details see FRITz & KRAINER, 2006, 2007). The Bom­ baso Formation crops out near Passo Pramollo (FRITz & KRAINER, 1995, 2006), Tomritsch (layers 1, 2, 5, 6) and Rudniggraben (KRAINER in VENTURINI, 1990b; FRITz & KRAINER, 2006). According to the authors, typical ele­ ments of the floras include Linopteris neuropteroides, Neu- ropteris cordata, N. scheuchzeri and N. ovata. Tomritsch 6 has been attributed to the Odontopteris cantabrica­zone, due to the presence of Sphenophyllum oblongifolium and Neuropteris scheuchzeri (moved to Macroneuropteris) following the mega­ flora­zonation of WAGNER (1984). This translates to a Can­ tabrian age (late Pennsylvanian; FRITz & KRAINER, 1995). The fossiliferous horizons of Malga (Alm) Straniger, Wai­ degger Alm, zollner See, Passo del Cason di Lanza and Tom­ ritsch 3 belong to the Meledis Formation. Tomritsch 3 has been attributed, due to the presence of Sphenophyllum angus- Figure 8: Location of the Permian-Carboniferous Carnic Basins of the Car- nic Alps (from VENTURINI, 1990b). PCP: Permo-Carboniferous sequence; VG: Val Gardena Sandstone. 1 and 2 are idealized and very schematic sec- tions respectively, outside and inside the Permo-Carboniferous basin areas. Figure 9: A general strati- graphic scheme of the Car boniferous-Permian units in the Carnic Alps (from VEN TURINI, 1990 b). The Auer nig Group is now called the Pramollo Group. Ronchi et al.: Pennsylvanian floras from Italy: an overview of the main sites and historical collections Geologia Croatica 307 tifolium and Pseudomariopteris busquetii, to the Sphenophyl- lum angustifolium­ zone, which according to WAGNER (1984), corresponds to a lower to middle Stephanian C age. One of the most prominent elements of this flora is Linopteris neuropteroides var. major, as well as a high abundance in frag­ ments of the Neuropteris cordata and N. ovata (FRITz, 1990; FRITz & KRAINER, 2006). VAI et al. (1980) attributed the formation to the Cantabrian (late Moscovian to early Kasimo­ vian, early Stephanian) (see also PITTAU et al., 2008a). The floras of the Pizzul Formation, (Rio Tratte/Gar­ nitzenberg (malga Auernig), Watschinger Alm, Rudniggsat­ tel, Ringmauer; Austria, FRITz & KRAINER, 2006), are characterized by the occurrence of Sigillaria brardii, Sphe- nophyllum angustifolium, Sph. oblonguifolium, Pecopteris Figure 10: Stratigraphic sections from the upper part of the Coro- na Formation (A3) and the basal Auernig Formation (A4). Section A is from the western side and sec- tion B from the southern side of the Monte Corona (from KRAI NER in VENTURINI, 1990b, mod.). Geologia Croatica 65/3Geologia Croatica 308 feminaeformis, Callipteris gigas, Pseudomariopteris bus- quetii and Poa-Cordaites linearis which attributes the flora to the Sphenophyllum angustifolium­zone (lower to middle Stephanian C; FRITz & KRAINER, 1994). The most important and fossiliferous formation of the Pramollo Group is the Corona Formation (Ofenalm, Kronalpe/ Monte Corona, Garnitzenalm/Malga Carnizza, Garnitz en sat­ tel, Gugga, Madritschenkopf, Schlanitzer Almweg, Treßdorfer Alm, Naßfelder Sattel/Passo Pramollo; FRITz & KRA INER, 2007). The most famous locality is Monte Corona (e.g., STACHE, 1874; FRECH, 1894; GEyER, 1897; FRITz, 1980, 1990; FRITz, et al. 1990; KRAINER, 1992; FRITz & KRAINER, 1993). The presence of Pseudomariopteris bus- quetii attributes these floras to the Sphenophyllum angustifolium­ zone, (lower to middle Stephanian C; FRITz & KRA INER, 1993). Linopteris neuropteroides and Neuropteris cordata seem to disappear in the upper part of the formation. The appearance of the genus Lebachia, an important conifer genus during the Permian, is of particular interest, and not described from any of the other Carboniferous floras of the Carnian Alps (FRITz & KRAINER, 1993, 2006). The last formations yielding Car­ boniferous floras in the Carnian Alps are the Auernig Forma­ tion, (Gugga, Garnitzenberg/Monte Carnizza, Schulter and Rattendorfer Alm) and the Carnizza Formation (KRAINER in VENTURINI 1990 b, pag. 96–98). The Cordaites are miss­ ing in the Auernig Formation, while the Autunian marker Cal- lipteris conferta (i.e now Autunia conferta) appears (FRITz & BOERSMA, 1983; FRITz & KRAINER, 2007). So far, there has been only one study of the palynoflora of this area (FRANCAVILLA, 1966). According to the au­ thor, the microflora is characterized by the spores Den- sosporites, Dictyotriletes, Lycospora and Verrucosisporites. Very interesting regional correlations and comparison between the Italian/Austrian Carboniferous and Permian flo­ ras could be also done in the future with neighboring countries such as Slovenia (KOLAR­JURKOVŠEK & JURKOVŠEK, 2012). 3. TUSCANY Pisani Mountains The Pisani Mountains are located along the so­called Mid­ dle­Tuscan Ridge, a regional morpho­structural high extend­ ing from the Apuan Alps to the Leoni Mountain (Fig. 14). The stratigraphic sections of the Pisani Mountains, near San Lorenzo of Vaccoli in North­Western Tuscany (Valle del Guappero), can be subdivided into two main sedimentary cy­ cles (RAU & TONGIORGI, 1974). The first is represented by the alluvial to lacustrine San Lorenzo Schists (Fig. 15), very rich in megafloras of Pennsylvanian to Cisuralian age. The overlying fluvial Asciano red breccias and conglomerates, are attributed to the Early Permian for regional correlations. Figure 11: Detailed location of the main fossil flora sites in the Italian and Austrian sides of the Carnic Alps (from VENTURINI, 1990b, mod.). Ronchi et al.: Pennsylvanian floras from Italy: an overview of the main sites and historical collections Geologia Croatica 309 Figure 12: Some examples of the Pennsylvanian megaflora of the Carnic Alps (with kind permission of Udine Museum). A. Annularia carinata; B. Pecop- teris sp.; C. Lilpopia raciborskii; D. Paripteris cf. linguaefolia; E., F. Acitheca polymorpha, G. Alethopteris sp.; H. Lepidodendron cf. subdichotum (determinations S. Opluštil). Specimens A, B, E, F and H from Mt. Corona (Pontebba, Udine); C from Casera Cordin Grande (Paularo, Udine); D and G from Casera Auernig (near the old landslide, Ponteb ba; Udine). Large collections from the graphite­rich metapelites and metasandstones of the San Lorenzo Schists were put together by SIGISMONDO DE BOSNIAKI (1837–1921) and CARLO DE STEFANI (1851–1924), at the end of 19th century (DE BOSNIAKI, 1894; DE STEFANI, 1901). The collection of plant fossils of DE STEFANI (~ 1.000 specimens), is stored at the Natural History Museum of Florence, and at the Mu­ seum of Natural History of Pisa University (see CIOPPI in MONECHI & ROOK, 2010 for details; Fig. 16); the palae­ ontological collection (7000 specimens of plants and ani­ mals) of DE BOSNIAKI (1894) is stored at the Museum of Natural History of Pisa University. Additional discoveries in the same area (Valentona, Monte Togi, Monte Vignale, Sasso Campanaro) enriched the collection of those two museums. Geologia Croatica 65/3Geologia Croatica 310 Figure 13: Stratigraphic sections from the Bombaso Formation (Pramollo Mb.: Tomritsch A) and basal Pramollo Group (Auernig Group auct) units (Meledis Formation or A1 Formation: Tomrisch B). In the inset, a location map of the two sections Tomritsch A and B.) (from KRAINER in VENTURINI, 1990b, mod.). A recent reorganisation of DE STEFANI’S collection shows a flora composed of lycopsids (Sigillaria, Lepidoden- dron), horsetails (Calamites, Asterophyllites, Annularia, Sphenophyllum), ferns (Acitheca, Cyathocarpus, Diplazites, Sphenopteris), seed ferns (Alethopteris, Callipteris), “cy­ cads”, Cordaites and conifers (Walchia; LANDI DEGLI IN­ NOCENTI et al., 2008; CIOPPI in MONECHI & ROOK, 2010). No further information exists on the collection of DE BOSNIAKI. DE BOSNIAKI (1894) attributed the floras to the Permian, while DE STEFANI (1984) attributed them to Ronchi et al.: Pennsylvanian floras from Italy: an overview of the main sites and historical collections Geologia Croatica 311 the Carboniferous. Fig. 17 shows a biostratigraphic and lithostratigraphic subdivision of the Pennsylvanian­Autunian succession, on the basis of different fossil floras found at various localities in the Valle del Guappero (from TRE­ VISAN, 1955 and RAU & TONGIORGI, 1974 in LANDI DEGLI INNOCENTI et al., 2008; mod.). It is suggested that these floras are similar to the Sardi nian flora of the San Giorgio basin described by COCOzzA (1967). The genera Annularia, Asterophyllites, Calamites, Callipte- ridium, Cordaites, Pecopteris, and Walchia, occur in both floras (LANDI DEGLI INNOCENTI et al., 2008; CIOPPI in MONECHI & ROOK, 2010; see Fig. 18). TONGIORGI unsuccessfully attempted to collect micro­palaeontological data in the area of the Pisani Mountains (LANDI DEGLI INNOCENTI et al., 2008). Marine fossils of inferred Penn­ sylvanian age, were recently discovered in the lower part of the San Lorenzo Schists at Montuolo (PANDELI et al., 2008). These discoveries indicate strong palaeoenvironmen­ tal analogies between this part of the San Lorenzo Schists and the coeval, coastal­neritic Iano Schists and sandstones Figure 14: A structural sketch of the Pisani Mountains A. Tectonic map; B. Geological map (From RAU & TONGIORGI, 1974; TONGIORGI et al., 1977). Geologia Croatica 65/3Geologia Croatica 312 cropping out near Volterra (COSTANTINI et al., 1998) and the Rio Marina Formation on Elba Island (PANDELI et al., 2008). Iano Eastward, south of the Arno River, in the neighbourhood of the village of Iano (near Volterra) (Fig. 19), the basal sedi­ mentary succession of the Iano Schists (Fig. 20) yielded, plant fossils, crinoids, bivalves and putative brachiopods of Stephanian age from some of the more pelitic beds (VAI & FRANCAVILLA, 1974; PANDELI, 1998). The plants belong to the lycopsids (Stigmaria), horse­ tails (Calamites, Annularia,) and ferns (Acitheca, Aspidiop- sis, Cyathocarpus, Diplazites; CIOPPI in MONECHI & ROOK, 2010) 4. SARDINIA Trans­tensional tectonics, which deeply affected the disman­ tling of the Variscan orogen, led to the opening of a number of intramontane basins, filled with lacustrine to alluvial sedi­ ments (RONCHI et al., 2008 and ref. therein; see Fig. 21). South-western Sardinia Clear evidence of the first post­orogenic clastic deposition on the island is represented by the reduced San Giorgio Ba­ sin sequence, which crops out in the Iglesiente subregion (Figs. 21 and 22), and has been studied in detail (COCOzzA, 1967; BARCA & COSTAMAGNA, 2003; see Fig. 23). The San Giorgio flora comprises for example Pecopteris arbo- rescens, Callipteridium pteridium, Neuropteris planchardi and Diksonites plueckenetii f. sterzeli. This flora is stored in the Carbonia Museum and in the Museo di Geologia e Pale­ ontlogia “D. Lovisato” of the Dipartimento di Scienze Chi­ miche e Geologiche of Cagliari. COCOzzA (1967) pro­ posed a late Stephanian age for it, based on the composition of the megafossils. The finer sediments of this basin yield­ ing a rich microflora have been attributed a late Westphalian and early Stephanian (A and B) age (DEL RIO & PITTAU in CASSINIS et al., 2000; PITTAU & DEL RIO, 2002b). The flora shows several endemic species, suggesting onset of a regional characterized Sardinian flora resulting from the isolation of Sardinia from southern Europe during the Penn­ sylvanian, (for more details see PITTAU et al., 2008b). Central-eastern Sardinia In central­eastern Sardinia (Fig. 21), there are two basins with transitional “Stephano­Autunian” macrofloras: the Lake Mulargia (Sarcidano subregion), and the Seui­Seulo/Mon­ tarbu (Barbagia di Seulo subregion; RONCHI et al. 2008; CASSINIS et al., 2003). The flora of Lake Mulargia, with taxa such as Callipteris conferta (now Autunia conferta), C. naumanni, Lebachia cf. hypnoides was originally dubiously ascribed to the late Autunian (FRANCAVILLA et al., 1977). In the Seui Basin and the adjacent Seulo Basin, outcrops with plant megafossils occur in the fine­grained sediments (CASSINIS et al., 2003). About 50 different species were described by LAMARMORA (1857), MENEGHINI (1857), PAMPALONI (1900) and ARCANGELI (1901) for more details see COMASCHI CARIA (1959). The flora has been attributed to the Pennsylvanian­Cisuralian period. Also a re­ cently collected flora with Annularia sphenophylloides, cf. Pecopteris arborcens, (?P. cyathea, Pecopteris sp., Pecop- teris sp. aff. hemitelioides, P. unita, Cordaites sp., Sigillaria brardi, and Artisia sp. has been ascribed to an interval span­ ning the latest Carboniferous to basal Early Permian (Autu­ nian; BROUTIN et al., 2000; CASSINIS et al., 2003). Figure 15: Lithotratigraphic column of the Palaeozoic–Carnian succession of the Pisani Mountains, (after RAU & TONGIORGI, 1974). Ronchi et al.: Pennsylvanian floras from Italy: an overview of the main sites and historical collections Geologia Croatica 313 Figure 16: A. Acitheca isomorpha (sample IGF 13164); B. Crossotheca pinnatifida (sample IGF 332P); C. Sphenophyllum oblongifolium (sample IGF 160P); D. Asterophyllites equiseformis (sample IGF 13142); E. Crossotheca pinnatifida (sample IGF 424P). With the kind permission of Elisabetta Cioppi (Museo di Storia Naturale dell’Università degli Studi di Firenze, Sezione di Geologia e Paleontologia). Geologia Croatica 65/3Geologia Croatica 314 A succession with a clear “early Autunian” age (i.e., basal Asselian) macro­ and microflora, is that of Guardia Pisano (Sulcis subregion, PITTAU et al., 2002a), whereas succession with “late Atunian” macro­ and microfloristic associations include those of Escalaplano, Perdasdefogu (Gerrei and Ogliastra subregions) and Lu Caparoni (Nurra subregion). For more information on such basins see also RONCHI et al. (1998) and CASSINIS et al. (2000). A com­ parative and chronostratigraphic correlation chart of the different Pennsylvanian, Permo­Carboniferous and Per­ mian basins of Sardinia was produced by RONCHI et al. (2008; see Fig. 25). Slightly different age­attributions for the latest Carbo­ niferous­Autunian basins are suggested by PITTAU et al. (2008b; Fig. 26) based on the microfloristic data. Given the microfloral composition, these authors distinguish four dif­ ferent palynological phases: Pteridophytic pre­ Striatiti pol­ len Phase (Westphalian C­Stephanian A); Florinites Phase (Stephanian/Autunian) with relatively dominant Cordaites pollen grains; Potonieisporites Phase (Asselian) with domi­ nant monosaccate pollen (Potonieisporites); Vittatina-Stri­ atiti pollen Phase (Asselian­(?)Sakmarian age). The flora of central­eastern Sardinia is stored at the Lovisato Museum at the Dipartimento di Scienze Chimiche e Geologiche of Cagliari and at the Natural History Museum of Florence (PAMPALONI collection). Figure 17: Chronological ordering of the main fossil sites of the San Loren- zo Schists formation according to TREVISAN (1955) and RAU & TONGIORGI (1974). TREVISAN (1955) indicated the index fossils for each fossil locality (from LANDI DEGLI INNOCENTI et al., 2008, mod.). Figure 18: Fossil floras from the Pisani Mountains. A. Main taxonomic groups of the De Stefani collection B. Percentages of the taxono mical groups of the fossil sites identified in the De Stefani collection. Va: Valentona; M. To: Monte Togi; Tr: Traina; M. Vi: Monte Vignale; M. Vi*: Monte Vignale (collected by Fucini); SC: Sasso Campanaro (after LANDI DEGLI INNOCENTI et al., 2008, mod.). Ronchi et al.: Pennsylvanian floras from Italy: an overview of the main sites and historical collections Geologia Croatica 315 According to BROUTIN (in RONCHI et al., 2008), the Montarbu flora (Barbagia di Seulo subregion), firstly sig­ nalled by SPANO (1976), is a hygrophyllous Stephanian­like assemblage, with the very fragmentary cf. Rhachiphyllum sp. looking as an “Autunian” callipterid. Thus, the age of the Montarbu flora is still not well constrained. From a palynological point of view, the Montarbu mi­ croflora is framed in the Potonieisporites Phase (PITTAU et al., 2008b), being represented by high numbers of Potonie i- sporites and Florinites and with a minor component rep­ resented by Plicatipollenites, Costapollenites and Vittatina pollen types. Thus, Voltziales, Cordaitales and, to a lesser extent, Peltaspermales appear to characterize the flora grow­ ing on dry or drained areas and slopes, in the surroundings of the lacustrine basin of Montarbu, at Seui and Seulo, whereas a hygrophillous flora of licophytes, sphenophytes and pterophytes, covered shorelake, banks, ponds and the alluvial plain. 5. LIGURIA In Western Liguria (Briançonnais units) the Late Palaeozoic volcano­sedimentary sequence begins with fine to coarse­ grained arkosic and quartzitic meta­sediments of continental origin, formed by reworking of the underlying orthogneissic Namurian(?) basement, some hundred metres thick (Lisio Formation). This is followed by widespread calc­alkaline rhyolitic–rhyodacitic ignimbrites (Case Lisetto Metarhyo­ lites) (VANOSSI et al., 1986; CORTESOGNO et al., 1988b), in turn covered by fluvial­lacustrine meta­conglomerates (Ollano Formation). This sequence of sedimentary units was generally as­ cribed to the Late Westphalian–Stephanian interval on the basis of old records of plant remains, among which were Senftenbergia (Pecopteris) elegans, Pecopteris nodosa, An- nularia longifolia (Pian del Fo, Viozene; PORTIS, 1887) and Odontopteris obtusa (Pietratagliata; SQUINABOL, 1887). In the second half of the 20th century, BLOCH (1966) dis­ tinguished the following forms in the Ollano Formation: Pecopteris plumosa dentata, Sphenopteris schatzlarensis, Imparipteris (Neuropteris) oblique and Lepidophyllum sp., together with traces of Neuropteris and Calamites, and at­ tributed the pertaining deposits to the late Westphalian (­Stephanian). According to the authors (e.g. VANOSSI et al., 1986), during the Pennsylvanian (Stephanian–?Autunian), lacu­ strine shales and siltstones (Murialdo Formation) or conti­ nental arenites (Viola and Gorra Schists) were deposited Figure 19: Generalized geological map of Iano (after COSTANTINI et al., 1998 and PANDELI, 1998). Figure 20: Lithotratigraphic column of the Carboniferous-Carnian succe- ssion of the Iano inlier (after COSTANTINI et al., 1998). Geologia Croatica 65/3Geologia Croatica 316 Figure 21: Location of the main Pennsylvanian and Permo-Carboniferous basins in Sardinia: 1) San Giorgio (Iglesiente subregion); 2) Tuppa Niedda (Ar- burese subregion); 3) Lake Mulargia (Sarcidano subregion); 4) Seui-Seulo (Barbagia di Seulo subregion); 5) Montarbu (Barbagia di Seulo) (from RONCHI et al., 2008, mod.). either on the Ollano Formation, or directly on the basement. This sedimentation is associated with the emplacement of andesite, and rare dacite lavas, and volcanic breccias, mainly in lacustrine basins. Tuffs and epiclastites of intermediate composition are widespread, also within continental arenites (Eze Formation). Elsewhere in the Penninic domain, Pennsylvanian mag­ matism is poorly represented, whereas the continental de­ posits, associated with strike­slip tectonics, are well develo­ ped, such as within the coeval sediments of the ‘zone Houiller Briançonnais’ (e.g. FABRE, 1961; BROUSMICHE­DEL­ CAMBRE et al., 1995 and ref. therein). Ronchi et al.: Pennsylvanian floras from Italy: an overview of the main sites and historical collections Geologia Croatica 317 Figure 23: Stratigraphic section of the Pennsylvanian San Giorgio Basin (from BARCA & COSTAMAGNA, 2003). Figure 22: Location and schematic stratigraphic section of the San Giorgio basin, close to Iglesias town, in the Iglesiente subregion (from DEL RIO & PITTAU, 2000). In contrast with such accepted age­determinations, and with all the former stratigraphic interpretations (see e.g., VANOSSI et al., 1986), the Pennsylvanian volcanic and sedi mentary clas­ tic deposits, which unconformably overlie a Namurian crystal­ line basement, have recently been related to Permian ages (DALLAGIOVANNA et al., 2009). New radioisotopic dates on the Case Lisetto rhyolites (285.6 ±2.6 Ma concordant age), ascribed these volcanic rocks to the late Sakmarian–?Artinskian time­span. Therefore the Ollano Formation should be placed in the Early Permian, in firm conflict with its palaeontological con­ tent, as reported in earlier literature. Shiny graphite­like features, found whitin Carbonife­ rous schists by DE STEFANI (1887a) on his excursions to Pietratagliata (Genoa), are stored in the Natural History Museum of Florence (CIOPPI in MONECHI & ROOK, 2010). 6. CONCLUSIONS The Italian Pennsylvanian continental successions are scat­ tered across the country in the following places: 1) In the western Southern Alps (Lombardy/Switzer­ land) sparse sections occur pitched in tectonic slices at the front of the metamorphic basement. The rich macroflora from the Alpe Logone has been dated to the Bolsovian (West­ phalian C), or Duckmantian­Bolsovian (Westphalian B–C transition). Between the Maggiore and Lugano lakes, the outcrops are less rich in plant remains, and perhaps slightly older than these of Logone. 2) In the eastern Southern Alps (Carnic Alps) the Car­ boniferous successions crop out in several localities near the border with Austria, such as Passo Pramollo, Cason di Lanza, Geologia Croatica 65/3Geologia Croatica 318 Figure 24: Plant fossils from the Pennsylvanian San Giorgio Basin (SW Sardinia). A. Calamites sp.; B. Sphenophyite strobili (cf. Cala mostachys); C. Annularia sp.; D. Neuropteris planchardii; E. Odontopteris sp., F. Dicksonites plueckenetii; G. Cordaites cf. lingulatus. Rio dai Amplis, Fontanone, Cima Val di Puartis, Monte Piz­ zul and Monte Corona. Although the flora has been studied partly on the Austrian side, the Italian outcrops are poorly studied. Plant fossils occur there in several formations of the Pramollo Group, but are especially abundant in the Corona Formation. The floras seem to have ages varying from Can­ tabrian up to lower to middle Stephanian. 3) In Tuscany, the floras mostly come from the Pisani Mountains and the surroundings of Iano. The San Lorenzo Schists, from which the specimens of the historic collections were collected, have been attributed to a Pennsylvanian to Cisuralian age. 4) Several small basins in Sardinia yield megafossils and/or palynomorphs respectively of Westphalian­Stepha­ Ronchi et al.: Pennsylvanian floras from Italy: an overview of the main sites and historical collections Geologia Croatica 319 Figure 26: Correlation hypothesis for lithostratigraphic units and Palyno- logical phases proposed for the continental succession of the Upper Car- boniferous and Lower Permian of Sardinia (from PITTAU et al., 2008b). Figure 25: Correlation chart of the main Pennsylvanian and Permo-Carboniferous basin of Sardinia (from RONCHI et al., 2008, mod.). The numbers below stage names represent the duration of the stages. nian, Stephano­Autunian or Autunian age, suggesting the differentiated onset of basins in Late Palaeozoic times in re­ lation to the Hercynian and moreover post­Hercynian tec­ tonic events. 5) The floras of Liguria mostly come from Pietratagliata (Genoa). This flora has a Late Westphalian–Stephanian age. ACKNOWLEDGEMENT The authors thank Luca SIMONETTO, Giuseppe MUSCIO (Museo Friulano di Storia Naturale of Udine), Elisabetta CIOPPI (Museo di Storia Naturale dell’Università degli Studi di Firenze, Sezione di Geologia e Paleontologia), Pao lo ARDUINI, Alessandro GARASSINO, Giorgio TERUzzI (Museo Civico di Storia Naturale di Milano) and Attilio SELVA (Museo Etnografico e Naturalistico Val Sanagra) for their help with the collections and obtaining information. The IGCP 575 group is also acknowledged for fruitful discussion and in particular Christopher J. CLEAL (Cardiff Museum), Stanislav OPLUŠTIL (Charles University, Prague) and Josef PŠENIČKA (West Bohemian Museum in Pilsen). The latter authors provided pictures and plant determinations of the Val Sanagra flora (from Venzo Collection hosted in Milano Mu­ seum) and of the Carnic Alps floras. Thanks also to the Museo Friulano di Storia Naturale of Udine, Museo di Storia Natu­ rale dell’Università degli Studi di Firenze, Lovisato Museum at the Dipartimento di Scienze Chimiche e Geologiche of Cagliari, for kindly providing some pictures of their plant fos­ sils. Giuseppe CASSINS (Pavia University) is warmly ac­ knowledged for his many inputs to revise the topic and for an early check of this paper. We due thanks also to Renato GIANOTTI (Pavia University) for sharing his knowledge on the Carboniferons outcrops of NW Italy. The authors thankfully acknowledge W. DIMICHELE (NMNH Smithsonian Institution, Washington) and an anon­ ymous reviewer for providing a constructive critical review. Two authors (A.R. and G.S) were supported by the PRIN 2008 funds (G. Oggiano coordinator). Geologia Croatica 65/3Geologia Croatica 320 REFERENCES ARCANGELI, G. (1901): Contribuzione allo studio dei vegetali permo­ carboniferi della Sardegna.– Paleont. It., 7, 91–120. ARTHAUD, F. & MATTE, P. (1977): Late Paleozoic strike­slip faulting in southern Europe and northern Africa: result of a right­lateral shear zone between the Appalachians and the Urals.– GSA Bull., 88, 1305–1320. doi: 10.1130/0016­7606(1977)88 BARCA, S. & COSTAMAGNA L. G. (2003): The Upper Carboniferous S. Giorgio succession (Iglesiente, SW Sardinia): stratigraphy, de­ positional setting and evolution of a late to post­Variscan molassic basin.– Boll. Soc. Geol. It., Volume speciale, 2 (2003), 89–98. BARCA, S., COSTAMAGNA, L.G. & DEL RIO, M. (1995b): Affiora­ menti permo­carboniferi e mesotriassici fra Porto Piscinas e Punta Acqua Durci (Arburese, Sardegna SW).– Boll. Soc. Sarda Sci. Nat., Sassari, 30, 1–11. BAGGIO, P. & DE MARCO, L. (1960): La serie basale tardo­paleozoi­ ca del varesotto e le mineralizzazioni ad uranio della Valganna. Stu­ di e Ricerche della Divisione Geomineraria, Comitato Nazionale Energia Nucleare, III, 15–103. BAUCON, A. & NETO DE CARVALHO, C. (2008): From the river to the sea: Pramollo, a new ichnolagerstätte from the Carnic Alps (Car­ boniferous, Italy–Austria).– Studi Trent. Sci. Nat. Acta Geol., 83, 87–114. BERNOULLI, D. (1964): zur Geologie des Monte Generoso (Lombar­ dische Alpen). Ein beitrag zur Kenntnis der Südalpinen Sedimente. Beiträge zur Geologischen Karte der Schweiz, Neue Folge 118 Lie­ ferung, 134 p. BERTOTTI, G. (1991): Early Mesozoic extension and Alpine shorten­ ing in the western Southern Alps: the geology of the area between Lugano and Menaggio (Lombardy, Northern Italy).– Mem. Sci. Ge­ ol., Padova, con 1 carta geologica, 43, 17–123. BLOCH, J.P. (1966): Le Permien du domaine briançonnais ligure. Essai de cronologie des formations ante triasiques. Atti del Symposium sul Verrucano, Pisa.– Atti Soc. Toscana di Scienze Naturali, Special Issue, 99–115. BROUSMICHE­DELCAMBRE, C., MERCIER, D. & COQUEL, R. (1995) : Implications stratigraphiques de la révision de la flore carbonifère au Sud de Brianc¸on.– C. R. Acad. Sci., Se´rie II, 320, 335–340. CASATI, P. (1978): Tettonismo e sedimentazione nel settore occidenta­ le delle Alpi Meridionali durante il tardo Paleozoico, il Triassico e il Giurassico.– Riv. It. Pal. Strat., 84, 313–326. CASSINIS, G., AVANzINI, M., CORTESOGNO, L., DALLAGIOVAN­ NA, G., DI STEFANO, P., GAGGERO, L., GULLO, M., MASSA­ RI, F., NERI, C., RONCHI, A., SENO, S., VANOSSI, M., SVEN­ TURINI, C. (1998): Synthetic Upper Palaeozoic correlation charts of selected Italian areas.– Atti Ticinensi di Scienze della Terra, 40, 65–120. CASSINIS, G., PEROTTI, C. & VENTURINI, C. (1997): Examples of late Hercynian transtensional tectonics in the Southern Alps (Italy).– In: DICKINS, J.M., yANG, z., yIN, H., LUCAS, S.G. & AN­ CHARyyA, S.K. (eds.): Late Palaeozoic and Early Mesozoic Cir­ cum­Pacific Events and Their Global Correlation. Cambridge University Press, Cambridge, 41–50. CASSINIS, G., CORTESOGNO, L., GAGGERO, L., PITTAU, P., RON­ CHI, A. & SARRIA, E. (Coordinators) (2000): Late Palaeozoic con­ tinental basins of Sardinia.– Field trip guidebook, 15–18 September, 1999. Inter. Field Conference on “The Continental Permian of the Southern Alps and Sardinia (Italy). Regional reports and general correlations”, 15–25 Sept. 1999, Brescia, p. 116. CASSINIS, G., CORTESOGNO, L., GAGGERO, L., RONCHI, A., SARRIA, E., SERRI, R. & CALzIA, P. (2003): Reconstruction of igneous, tectonic and sedimentary events in the latest Carbonifer­ ous–Early Permian Seui Basin (Sardinia, Italy).– In: DECANDIA, F.A., CASSINIS, G. & SPINA, A. (eds): Spec. Proc. Int. Meeting “Late Palaeozoic to Early Mesozoic events of Mediterranean Eu­ rope, and additional regional reports”, Siena, 2001. Boll. Soc. Geol. It., vol. Spec., 2, 99–117. CASSINIS, G. & PEROTTI, C.R. (2007): A stratigraphic and tectonic review of the Italian Southern Alpine Permian.– Palaeoworld, 16/1–3, 140–173. doi: 10.1016/j.palwor.2007.05.004 CASSINIS, G. & RONCHI, A. (2002): The (late­) Post­Variscan conti­ nental succession of Sardinia.– Rend. Soc. Pal. Ital., 1, 77–92. COCOzzA, T. (1967): Il Permo­Carbonifero del bacino di San Giorgio (Iglesiente, Sardegna sud­occidentale).– Mem. Soc. Geol. It., 6, 6–642. COMASCHI CARIA, I. (1959): Le piante fossili della Sardegna. Mem. Riv. It. Pal. Strat., 7, 1–176. CORTESOGNO, L., DALLAGIOVANNA, G. & VANOSSI, M. (1988a): Paléogéographie du Briançonnais ligure d’après les lithoclastes des formations permo­carbonifères.– Géologie Alp., Mém. h.s., 14, 9–28. CORTESOGNO, L., DALLAGIOVANNA, G., VANNUCCI, R. & VA­ NOSSI, M. (1988b): Volcanisme, sédimentation et tectonique pen­ dant le Permo­Carbonifère en Briançonnais Ligure: Une revue. Eclogae Geol. Helv., 81, 487–510. COSTANTINI, A., ELTER, F.M., PANDELI, E. & SANDRELLI, F. (1998) : Geologia dell’ area di Iano (Toscana meridionale, Italia).– Boll. Soc. Geol. It., 117, 187–218. DALLAGIOVANNA, G., GAGGERO, L., MAINO, M., SENO, S. & TIEPOLO, M. (2009) : U–Pb zircon ages for post­Variscan volca­ nism in the Ligurian Alps (Northern Italy).– J. Geol. Soc. Lond., 166, 101–114. doi: 10.1144/0016­76492008­027 DE STEFANI, C. (1901): Flore carbonifere e permiane della Toscana.– Pubbl. Reg. Ist. Studi Sup. Pratici e Perfez., Tipografia G. Carne­ secchi e Figli, Firenze, 212 p. DEL RIO, M. (1973): Palinologia di un vello “permo­carbonifero” del bacino di San Giorgio (Sardegna sud­occidentale).– Boll. Soc. Geol. It., 93, 485–494. DEL RIO, M. & PITTAU, P. (2000): The Upper Carboniferous of the San Giorgio basin (Iglesiente).– In: CASSINIS, G., CORTESO­ GNO, L., GAGGERO, L., PITTAU, P., RONCHI, A. & SARRIA, E. (eds.): Late Paleozoic continental basins of Sardinia. Field trip guidebook, 15–18 September, 1999. Field Conference on: “The Continental Permian of the Southern Alps and Sardinia (Italy). Re­ gional reports and general correlations”. ESCHER, B.G. (1911): Über die prätriasische Faltung in den West­alpen. Diss, zürich. FRANCAVILLA, F. (1966): Spore nel Flysch Hochwipfel.– Giornale di Geologia, 2, 493–526. FRECH, F. (1894): Die Karnischen Alpen. Ein Beitrag zur vergleichen­ den Gebirgstektonik.– Halle (Max Niemeyer), 514 p. FRITz, A. (1980): Fundberichte über Pflanzenfossilien aus Kämten 1980.– Carinthia II, 170(90), 221–238. FRITz, A. & BOERSMA, M. (1983): Fundberichte über Pflanzenfossi­ lien aus Kämten.– Carinthia II, 173(93), 19–41. FRITz, A. & BOERSMA, M. (1987): Fundberichte über Pflanzenfossi­ lien aus Kämten 1987 – Beitrag 15: Wunderstätten (Unterperm), St. Pauler Berge.– Carinthia II, 177(97), Jahrgang, 381–394. FRITz, A., BOERSMA, M. & KRAINER, K. (1987): Steinkohlenzeit­ liche Pflanzenfossilien aus Kämten.– 49. Sonderheft des naturwis­ senschaftlichen Verreins für Kämten, Klagenfurt, 89 p. FRITz, A., BOERSMA, M. & KRAINER, K. (1990): Carinthia II, Sonderheft, 4, 120. FRITz, A. & KRAINER, K. (1994): Die Megflora “Garnitzenberg­Süd­ os alpha” aus der Auernig­Schichtgruppe der Karnischen Alpen.– Carinthia II, 441–465. Ronchi et al.: Pennsylvanian floras from Italy: an overview of the main sites and historical collections Geologia Croatica 321 FRITz, A. & KRAINER, K. (1995): Die Megaflora Tomritsch­3 und Tomritsch­6 aus den oberkarbonen Auernigschichten der Karni­ schen Alpen.– Carinthia II, 553–583. FRITz, A. & KRAINER, K. (2004): Pflanzenfossilien aus den Grenz­ landbänken der Rattendorfer Alm (Kernten, Karnische Alpen).– Ca­ rinthia II, 194(114), Jahrgang, 445–454. FRITz, A. & KRAINER, K. (2006): Vegetationsgeschichtliche und flo­ rengeographische Untersuchungen im Oberkarbon und Unterperm der Ost­ und Südalpen (Teil 1).– Carinthia II, 196(116), 93–120. FRITz, A. & KRAINER, K. (2007): Vegetationsgeschichtliche und flo­ rengeographische Untersuchungen im Oberkarbon und Unterperm der Ost­ und Südalpen (Teil 2).– Carinthia II, 197(117), 91–148. FRITz, A. & KRAINER, K. (1993): Eine neue Megaflora aus dem Ste­ fan der Kronalpe.– Carinthia II, 485–517. FRITz, A. & UCIK, F.H. (2003): Neufunde von Pflanzenfossilien aus Kämten.– Carinthia II, 193(113), 449–454. GAETANI, M., GIANOTTI, R., JADOUL, F., CIARAPICA, G., CIRIL­ LI, S., LUALDI, A., PASSERI, L., PELLEGRINI, M. & TANNO­ IA, G. (1986): Carbonifero superiore, Permiano e Triassico nell’area Lariana.– Mem. Soc. Geol. It., 32, 5–48. GEyER, G. (1897): Über dei geologsichen Verhältnisse im Pontafeler Abschnitte der Karnischen Alpen.– Jahrbuch der k.k. Geol. R.A., p. 46. GRAETER, P. (1951): Geologie und Petrographie des Malcantone (Süd­ liches Tessin).– Schweiz. Mineral. Petrogr. Mitt., 31/2, 361–483. HEER, O. (1876): Flora fossilis Helvetiae, 47. Verlag von J. Wurster and Co., zurich, 41–42. JONGMANS, W.J. (1950): Mitteilungen zur Karbonflora der Schweiz. I.– Eclogae geol. Helv., 43/2, 95–104. JONGMANS, W.J. (1960): Die Karbonflora der Schweiz. Beiträge zur geologiche Karte der Schweiz (NF), 108, 1–97. KOLAR­JURKOVŠEK, T. & JURKOVŠEK, B. (2012): Late Carbonerous floras in Slovenia – a review, 65/3, 323–328. doi: 104154/gc.2012.21 KRAINER, K. (1990): The fossil flora of the Auering Group.– Field Workshop on Carboniferous to Permian Sequence of the Pramollo­ Nassfeld Basin, 110–113. LAMARMORA, A. (1857): Voyage en Sardaigne: troisième partie. Des­ cription géologique et paléontologique. Torino, Bocca Impr. Royale, 2, 707–781. LANDI DEGL’INNOCENTI, V., PANDELI, E., MARIOTTI LIPPI, M. & CIOPPI, E. (2008): The Carboniferous­Permian succession of the Pisani Mountains (Tuscany, Italy): preliminary data from the De Stefani collection (Natural History Museum of Florence).– Boll. Soc. Geol. It. (Ital. J. Geosci.), 127/3, 545–558. LEHNER, P. (1952): zur Geologie des Gebietes der Denti della Vecchia, des M. Broglia, des M. Brè, und des M. San Salvatore bei Lugano.– Eclogae geol. Helv., 45, 86–159. MAGNANI, M., (1946): Sulla presenza di terreni spettanti al Carboni­ fero nei monti di Menaggio (Valle Sanagra). Atti della Regia Ac­ cademia delle Scienze di Torino 80, I, 199–206. MASSARI, F., PESAVENTO, M. & VENTURINI, C. (1991): The Per­ mian Carboniferons cyclothenis of the Pramollo Basin Sequence (Carnic Alps).– In: VENTURINI, C. (ed.): Field Workshop on Car­ boniferous to Permian sequence of the Pramollo­Nassfeld Basin (Carnic Alps), Guidebook, 171–185. MENEGHINI, G. (1857) : Paléontologie de l’île de Sardaigne.– In: LAMARMORA, A. (ed.): Voyage en Sardaigne, IV, Paris. MONECHI, S. & ROOK, L. (2010): The Museum of Natural History of the University of Florence. The Geological and Paleontological Collections ISBN 978­88­6453­189­2 (print) © 2010 Firenze Uni­ versity Press. OPLUŠTIL, S. & CLEAL, C.J. (2007): A comparative analysis of some Late Carboniferous basins of Variscan Europe.– Geol. Mag., 144, 417–448. doi: 10.1017/s0016756807003330 PAMPALONI, L. (1900): I terreni carboniferi di Seui ed oolitici di Per­ daliana.– Red. Acc. Lincei., Cl. Sc. Sif. Math. e Nat., 9/2, 345–349. PANDELI, E. (1998): Permo­Triassic siliciclastic sedimentation in the northern Apennines: new data from the Iano metamorphic Inlier (Florence).– Mem. Soc. Geol. It., 53, 185–206. PANDELI, E. (2002): Sedimentary­tectonic evolution of the Tuscan ar­ ea (Northern Apennines, Italy) fro Late “Autunian” to Carnian.– Boll. Soc. Geol. It., Vol. Spec., 1, 251–262. PANDELI, E., DOMINICI, S., LANDI DEGL’INNOCENTI, V., CIOP­ PI, E. & TANGOCCI, F. (2008): Marine fossils in the Late Carbon­ iferous metasediments of the Pisani Mountains (Tuscany, Italy).– Boll. Soc. Geol. It. (Ital. J. Geosci.), 127/3, 559–565. PITTAU, P. & DEL RIO, M. (2002): Palynofloral biostratigraphy of the Permian and Triassic sequences of Sardinia.– Rend. Soc. Pal. It., 1, 93–109. PITTAU, P., BARCA, S., COCHERIE, A., DEL RIO, M., FANNING, M. & ROSSI, P. (2002): Le bassin permien de Guardia Pisano (Sud­ Ouest de la Sardaigne, Italie): palynostratigraphie, paléo phyto géo­ gra phie, corrélations et âge radiométrique des produits volcani­ ques as sociés. Geobios, 35, 561–580. doi: 10.1016/s00166995(02) 00069­4 PITTAU, P., DEL RIO, M., COTzA, F., RONCHI, A., SANTI, G., & GIANOTTI, R. (2008a): Pennsylvanian miospore assemblages from the Bèdero Section, Varese, Italian Southern Alps.– Revue de mi­ cropaléontologie, 51, 133–166 doi: 10.1016/j.revmic.2007.11.001. PITTAU, P., DEL RIO, M. & FUNEDDA, A. (2008b): Relationships between plant communities characterization and basin formation in the Carboniferous­Permian of Sardinia. Boll. Soc. Geol. It. (Ital. J. Geosci.), 127/3, 7–653. PORTIS, A. (1887): Sulla scoperta delle piante fossili carbonifere di Vio­ zene nell’alta valle del Tanaro.– Boll. R. Com. Geol. It., 18, 417–420. RAU, A. & TONGIORGI, M. (1974): Geologia dei Monti Pisani a sud­ est della Valle del Guappero.– Mem. Soc. Geol. It., 13, 227–408. RONCHI, A., BROUTIN, J., DIEz, J­B., FREyTET, P., GALTIER, J. & LETHIERS, F. (1998): New palaeontological discoveries in some Early Permian sequences of Sardinia. Biostratigraphic and palaeo­ geographic implications.– C. R. Acad. Sci. Paris, Earth & Planet. Sci., 327, 713–719. doi:10.1016/s1251­8050(99) RONCHI, A., SARRIA, E. & BROUTIN, J. (2008): The “Autuniano Sar do”: basic features for a correlation through the Western Medi­ terranean and Paleoeurope.– Boll. Soc. Geol. It., 127/3, 655–681. SELLI, R. (1963): Schema geologico delle Alpi Carniche e Giulie occi­ dentali.– Giornale di Geologia, 2/30, 1–136. SORDELLI, F. (1896): Flora fossile insubrica. Studi sulla vegetazione in Lombardia durante i tempi geologici.– Tipografia Cogliati Mila­ no, 298 p. SPANO, C. (1976): Nuovo contributo alla conoscenza delle piante del Paleozoico della Sardegna.– Rend. Seminari Fac. Sci. Univ. Caglia­ ri, 46/3–4, 385–433. SQUINABOL, S. (1887): Nota preliminare su alcune impronte fossili nel carbonifero superiore di Pietratagliata. Giornale della Societa’ di Letture e Conversazioni Scientifiche di Genova 10/6–7. Tipogra­ fia di Gaetano Schenone, Genova. STACHE, G. (1874): Die paläozoischen Gebiete der Ostalpen.– Jb. der k.k. Geol. R.A., 24/2. STADLER, G., TEICHMULLER, M. & TEICHMULLER, R. (1976): zur geotermischen Geschichte des Karbons von Manno bei Lugano des “Karbons” von Falletti (Sesia­zone der Westalpen).– N. Jb. Geol. Paleont. Abh., 152, 177–198. TONGIORGI M., RAU, A. & MARTINI, I.P. (1977): Sedimentology of Early­Alpine, fluvio­marine clastic deposits (Verrucano, Triassic) in the Monti Pisani (Italy).– Sediment. Geol., 17, 311–332. doi: 10.1016/0037­0738(77)90051­3 Geologia Croatica 65/3Geologia Croatica 322 VAI, G.B. & FRANCAVILLA, F. (1974): Nuovo rinvenimento di piante dello Stefaniano a Iano (Toscana).– Boll. Soc. Geol. It., 93, 73–79. VAI, G.B., FRANCAVILLA, F., FERRARI, A. & CONTARIN, M.T. (1980): La sezione del Monte Carnizza (Carbonifero superiore, Alpi Carniche).– Mem. Soc. Geol. It., 20, 267–276. VAI, G.B. & VENTURINI, C. (1997): Moscovian and Artinskian rocks in the frame of the cyclic Permo­Carboniferous deposits of the Car­ nic Alps and related areas.– Geodiversitas, 19, 173–186. VAN AMEROM, H.W.J. & KABON, H. (2000): Neue fossile Floren aus dem Nötscher Karbon (2. Teil).– Carinthia II, 190(110), 483–516. VAN AMEROM, H.W.J. & SCHÖNLAUB, H.P. (1992): Pflanzenfossili­ en aus dem Karbon von Nötsch und der Hochwipfel­Formation der Karnischen Alpen (Österreich).– Jb. Geol. B.­A., 135/1, 195–216. VAN AMEROM, H.W.J., BOERSMA, M. & RIEHL­HERWIRSCH, G. (1976a): zum Alter des “Karbons von Christophberg”, Kämten, Östeich.– Geologie en Mijnbouw, 55/3–4, 211–212. VAN AMEROM, H.W.J., BOERSMA, M., NIEDERMAyR, G. & SCHERIAU­NIEDERMAyR, E. (1976b): Das permische Alter der “Kar bon”­Flora von Kötschach (Kärnten, Österreich).– Carinthia II 166 (86), 93–101. VANOSSI, M., CORTESOGNO, L., GALBIATI, B., MESSIGA, B., PICCARDO, G.B. & VANNUCCI, R. (1986): Geologia delle Alpi Liguri: dati, problemi, ipotesi.– Mem. Soc. Geol. It., 28, 5–75. VENTURINI, C. (1983): Il bacino tardo­ercinico di Pramollo (Alpi Car­ niche): un’evoluzione regolata dalla tettonica sinsedimentaria.– Mem. Soc. Geol. It., 24, 23–42. VENTURINI, C. (1990a): Geologia delle Alpi Carniche centro­orientali. Pubblicazione 36, Museo Friulano di Storia Naturale, Udine, 220 p. VENTURINI, C. (1990b): Field Workshop on Carboniferous to Permian Sequence of the Pramollo­Nassfeld Basin (Carnic Alps), Guide­ book. Arti Grafiche Friulane, Udine, 159 p. VENTURINI, C. (1991): Introduction to the geology of the Pramollo Ba­ sin (Carnic Alps) and its surroundings.– In: VENTURINI C. (ed.): Workshop Proceedings on Tectonics and Stratigraphy of the Pramol­ lo Basin (Carnic Alps).– Giorn. Geologia, ser. 3a, 53/1, 13–47. VENTURINI, C. (2002a): La sequenza permo­carbonifera.– In: AA.VV. Guide Geologiche Regionali – Alpi e Prealpi Carniche e Giulie, Friuli Venezia Giulia, a cura della Società Geologica Italiana, 9, 20–31, BE­MA editrice. VENTURINI, C. (2006): Evoluzione geologica delle Alpi Carniche. Pub­ blicazione 48, Edizioni del Museo Friulano di Storia Naturale – Co­ mune di Udine, 208 p. VENTURINI, C., PONDRELLI, M., DELzOTTO, S., FONTANA, D. & DISCENzA, K. (2002): Carta geologica delle Alpi Carniche (scala 1:25.000, 930 kmq). S.E.L.C.A., Firenze. VENTURINI, C., KRAINER, K. & MASSARI, F. (1991): Field trips in the Pramollo basin (Carnic Alps).– In: VENTURINI, C. (ed.): Workshop Proceedings on Tectonics and Stratigraphy of the Pramollo Basin (Carnic Alps). Giornale di Geologia, ser. 3a, 53/1, 49–126. VENzO, S. (1951): Les gisements nouveaux du Carbonifère (Westpha­ lien) dans les Alpes Lombardes. C. R. du 31e Congrès de Stratigra­ phie et de Géologie du Carbonifère. Herleen 1951, 647–649. VENzO, S. & MAGLIA, L. (1947): Lembi carboniferi trasgressivi sui micascisi alla “Fronte sedimentaria subalpina” del Comasco (Ac­ quaseria di Menaggio­Bocchetta di S. Bernardo) e del Varesotto (Bèdero). Atti Soc. It. Sci. Nat., 85/86, 33–70. WAGNER, R.H. (1984): Megaflora zones of the Carboniferous.– C.R. IX. Congr. Int. Stratigr. Geol. Cerbonifère, Washington and Cham­ paign­Urbana 1979, 2, 9–134. Manuscript received August 02, 2012 Revised manuscript accepted September 21, 2012 Available online October 30, 2012