ACTA GEOLOGICA HISPANICA, v. 25 (1990), nV-2, phgs. 3-12 PROJECT 276
the Tethys
Paleozoic stratigraphy of the Central and Northern part of the Catalonian Coastal Ranges (NE Spain)
M. JULIVERT and H. DURAN
Univ. Autónoma de Barcelona, Dpt. de Geologia, 08193 Bellaterra (Barcelona, Spain)
ABSTRACT carbonífera. Las rocas mis antiguas que afloran forman una suce- sión esencialmente de esquistos, areniscas de grano fino, gneises The Paleozoic stratigraphic succession in the Catalonian Coastal (intrusiones laminares pre-hercinianas), mármoles, orto- y para- Ranges spans the interval from Cambrian(?) to Carboniferous, with anfibolitas y rocas calcosilicatadas. Una comparación con otras only one break, separating the pre-Carboniferous part of the sequence localidades permite asignar a estas rocas una edad del Cámbrico from the Carboniferous. The oldest rocks exposed form a sequence inferior (o tal vez mas antigua, en parte). Hacia arriba, la serie se of schists, fine grained sandstones, gneisses (laminar pre-Hercynian hace más monótona y pasa a una alternancia de esquistos (o pizarras intrusions), marbles, orto- and para-amphibolites and calcsilicate donde el grado metamórfico es menor) y capas delgadas de areniscas rocks. comparison with other localities iuggests an Early Cambrian de grano fino (Cámbrico-Ordovicico). Por encima, se encuentra una age (or perhaps in part older). Upwards the sequence becomes more sucesión de grauvacas y pizarras, con niveles de cantos englobados monotonous andconsists only of schists (or slates where themetamorphic en una matriz pelítica, intercalados cerca de su base y con niveles de grade is lower) and thin fine-grained sandstone layers (Cambrian- rocas volcánicas distribuidas por toda la sucesión. Este conjunt0 ha Ordovician). Still higher in the sequence, an altemation of greywackes proporcionado las faunas mis antiguas de las Cadenas Costeras and slates is found, with interlayered mud-supported conglomerates Catalanas, que indican una edad del Caradoc. Finalmente, en su at its lower part and acid volcanic rocks which occur throughout the parte mas alta, la sucesión ordovícica contiene unas delgadas capas whole sequence. This part of the sequence has provided the oldest de caliza que han proporcionado faunas del Ashgill. El Sildrico,del faunas known in the Catalonian Coastal Ranges, which indicate the Llandovery al Ludlow inferior, consiste en pizarras negras con sills Caradoc. Finally, in its uppermost part, the Ordovician sequence de doleritas, mientras que el Ludlow superior, el Pridoliense y el contains some thin limestone layers that contain Ashgill faunas. The Devónico inferior están formados por calizas nodulosas y margas Silurian, from Llandovery to Lower Ludlow, consists of black ricas en faunas pelágicas y hemipelágicas. Los niveles mas modernos graptolitic shales with dolerite sills, whilst the upper Ludlow, del Devónico que se han reconocido corresponden en general al Pridolian and Devonian consist of nodular limestones and marls Emsiense. La existencia de una discontinuidad estratigráfica con el withpelagic and hemipelagic faunas. The youngest Devonian faunas Carbonifero permite pensar que existia un Devónico mas completo found correspond in general to the Emsian. The existence of a gap que ha sido-erosionado. El carbonífero se caracteriza por estar at this point of the sequence suggests the possibility that part of the formado esencialmente Dorunaespesa sucesión de tip0 culm (Viseense- Devonian could have been eroded. The Carboniferous is characterized Westfaliense?), que seAapoyasobre unos delgadosniveles de liditas by a thick culm sequence (Visean to Westphalian?), resting on thin y de calizas (Tournaisiense y Viseense). Una comparación con 10s chert and limestone layers (Tournaisian and Visean). A comparison otros macizos paleozoicos alrededor del Meditarráneo occidental with neighbouring areas shows a similarity regarding succession pone de manifiesto la existencia de una gran similitud tanto en el and facies with other Paleozoic massifs around the Western Mediterranean. tip0 de sucesión como en las facies.
Key words: Catalonian Coastal Ranges. Paleozoic stratigraphy. Palabras clave: Cadenas Costeras Catalanas. Paleozoico.
INTRODUCTION RESUMEN The Paleozoic stratigraphical sequence in the Cata- La serie estratigráfica paleozoica en las Cadenas Costeras Cata- lanas comprende desde un probable Cámbrico al Carbonifero, si lonian Coastal Ranges can be divided into two sepa- bien con una interrupción, que separa la serie pre-carbonifera de la rate parts divided by a disconformity (or may be by an Figure 1.- Geological sketch of the Catalonian Coastal Ranges. 1, Gavarres. 2, Guilleries. 3, Montseny. 4, Montnegre. 5, Collcerola (Tibidabo). 6, Pedritxes. 7, Capellades area. 8, Serra de Miramar. 9, Priorat-Prades block.
angular unconformity). These parts are: 1) the pre- The pre-Silurian sequence is rather monotonous Carboniferous sequence, forming a conformable suc- and almost unfossiliferous. The oldest known faunas cession from the lower Cambrian (?) to the lower correspond to the Caradoc and have been found only in Devonian, and, 2) the Carboniferous, essentially formed a few localities. The scarcity of pre-Silurian faunas, by a thick terrigenous sequence (culm facies). together with strong deformation, abundance of gran- Pre-Carboniferous rocks are mainly found from itoids and lack of good mapable horizons in the pre- Barcelona to the north, separated in severa1 areas by Silurian sequence, have been the reasons for the slow late Hercynian granitoids and by Mesozoic and Terti- progress in the knowledge of the Paleozoic stratigra- ary cover sediments (Fig. 1). Carboniferous rocks phy since the early papers by Almera (1891, 1896, crop out mainly in the southernmost part of the Catalonian 1901) and Barrois (1893, 1913), and the synthesis by Coastal ranges (Priorat-Prades). Faura Sans (1913), Schriel (1929) and Ashauer and Teichmüller (1935). However, during the last decade Paleozoic rocks were affected by polyphase defor- active research has been in progress on the structure, mation and metamorphism during the Hercynian oro- metamorphism, plutonism, volcanism and metalog- geny. However, high-grade metamorphism is retricted eny of the Catalonian Coastal Ranges. Severa1 areas to small areas (southern Guilleries and southwestern have been carefully mapped and a new search for Montseny) in the lowest stratigraphical levels. Most Caradoc, Silurian and Devonian faunas has been un- rocks in the Catalonian Coastal Ranges have suffered dertaken (Julivert 1989; Julivert et al. 1985,1987; Villas meta.morphism under greenschist facies conditions, et al. 1987; Garcia-López et al. 1990). and the highest part of the stratigraphical sequence (Carboniferous) either lack metamorphism or has at In this paper, the Paleozoic stratigraphy of the most undergone anchimetamorphism. central and northern Catalonian Coastal Ranges will be presented, giving the general sequence for the trol. Two possibilities for correlation exist: 1) a Ranges and also some local successions on the most correlation with the Cambrian carbonate formation of representative localities. Attention will be focussed northwestern Spain (Láncara-Vegadeo Formation, Early on the pre-Carboniferous rocks, although a brief de- and Middle Cambrian), central Spain or the Iberian scription of the small Carbonifeorus outcrops existing Chain (Navalucillos Limestone and Ribota Dolostone will also 'be included. respectivelly, Late Early Cambrian), and 2) a correlation with the carbonates of the Carnbrian-Precambrianboundary or the uppermost Precambrian (carbonates in the lower part of the Herreria-Candana Formation in northwest- CAMBRIAN AND ORDOVICIAN ern Spain, carbonates near the Precambrian-Cambrian The oldest rocks are exposed in the southern part of boundary in central Spain). Les Guilleries and the southwestern part of the Montseny Upwards, the sequence becomes monotonous and massifs (Fig. 2). They form essentially a succession of consists only of schists (or slates, where the metamor- schists with interlayered fine-grained sandstones, phism decreases) with interbedded fine-grained sand- gneisses, marbles, amphibolites and calcsilicate rocks. stone layers. This sequence likely forms most of the Some of these rocks have been known since last cen- Montseny massif, between its southeastern part where tury (Vidal, 1886; Faura Sans, 1913); however, a the marbles and gneisses are exposed and its north- systematic survey was not undertaken unti1 severa1 western part where Caradoc fossils have been found decades later (Van der Sijp, 1951; Viladevall, 1978). and where the upper Ordovician could be mapped. In A detailed study has been carried out more recently by the northern part of the Montseny, and at a lower Durán (1985,1990) in Les Guilleries and Huerta (1989) position than the faunas, laminated facies exist which in the southwestern part of the Montseny massif. could be compared to the Jujols Formation of the The sequence can be best observed at Les Guiller- Pyrenees. In any case, the first Caradoc fossils occur ies. In this massif, the gneisses apparently form con- (perhaps more than 1000 m) above the carbonate cordant bodies, representing pre-Hercynian sheet-shaped horizon found in southeastern Montseny. intrusions and/or volcanic material. The gneisses seem to form severa1 layers, and the main body separates In the Montseny massif, the uppermost part of the two units named by Durán (1986, 1990) the Osor and Ordovician sequence (Figs. 2 and 3) consists of a 30- Susqueda formations. The Osor Formation, exposed 60 m thick horizon of grey-green slates (or shales) below the gneisses, consists of schists, amphibolites somewhat sandy, which in its upper part contains and some calcsilicate layers. The Susqueda Formation brachiopod and bryozoa fauna. A few metres above consists of interlayered schists and fine-grained sand- this fauna is a thin limestone bed (10-30 cm). This bed, stones, with a 20 m thick marble horizon some 50 although discontinuous, can be followed fairly easily metres above the top of the gneisses. Marbles, proba- in the Avenc6 creek area. Above the limestone bed bly corresponding to the same horizon, and gneisses there are some 100 m of dark-grey pelites with a pencil similar to those of Les Guilleries are also found in the structure formed due to the intersection of a weak southwestern part of the Montseny massif (IHuerta, cleavage with a diagenetic foliation parallel to bed- 1989). ding. Above, the typical black graptolite bearing Sil- urian shales are found. All the above quoted rocks show a metamorphism above the andalusite isograde, and in Les Guilleries The described sequence can be compared to that of even the sillimanite/K-feldspar zone is reached. In the Pyrenees, and possibly correlated with it. The consequence, no fossils are found and the ages must be limestone bed corresponds to the Estana Limestones, assigned by comparison. A comparison with the Pyr- the shales above to the Ansovell Formation, and the enees (Cavet, 1957; Hartevelt, 1970) shows a strong fossiliferous beds below to the Cavi Formation. The similarity between the Susqueda and the Canavelles boundary between Cavi and Jujols, outlined in the formations. However, as in the Catalonian Coastal Pyrenees by a conglomerate horizon (Rabassa Con- Ranges, no fossils older than the Caradoc have ever glomerate; Hartevelt, 1970), can not be traced at present been found in the central and eastern Pyrenees. Their in the Montseny massif. The ages assigned could be age has been tentativelly assigned to the Cambrian, by the same as in the Pyrenees. The brachiopod fauna lithological comparison (existence of a carbonate ho- found below the limestone horizon indicates an age rizon) with the Montagne Noire and the Iberian mas- between the Late Caradoc and the Middle Ashgill, the sif. However, an age assignment based upon the existence limestones may be Asghill, and the shales above could of a major carbonate unit is doubtful, since more than be Ashgill and/or Silurian. A list of the species found one carbonate horizon occurs in the Cambrian (and and a discussion on their stratigraphical implications very Late Precambrian ?) of neighbouring Hercynian can be found in the papers by Villas et al. (1987) and domains, where there is a better paleontological con- Julivert et al. (1987). PEDRITXES
Figure 2.- Paleozoic stsatigraphic sequences of the Catalonian Coastal Ranges, based on Durán (1985, 1990; Guilleries), Huerta (1990; Southeast Montseny), Ubach (1990, Pedritxes), Serra (1990; Capellades), and Julivert and Durán (1981, Tibidabo, and this paper, Northwest Montseny). F, fault.
6 DEVONIAN 1 ... Limestonn. mans and shaks
PR'D0L' Nodular limestom LOCHKOVl- AN
SILURIAN BIack prapldilic slates
Limrs lones ......
......
......
Figurc 3.- ticologiccll niap ol thc IIOI.I~IMC~~~I.IIPUI u1 tllc M~I~LSCIIYlnabs~l (Avenc6 creek area)
In the Guilleries massif the sequence is somewhat Ashgill age. For a more complete discussion and the different. The upper part of the Ordovician is formed list of species found the reader is referred to the papers by a sequence of greywakes, slates, acid volcanic by Villas et al. (1987) and Julivert et al. (1987). rocks (Durán, 1990; Durán et al. 1984) and some layers of mud-supported conglomerates near its base (Puig A comparison with the Pyrenees makes possible Sa Calm Formation of Durán, 1990, about 1000 m the correlation of the sequence containing acid vol- thick). Belaw the conglomerates, there is an alterna- canics with the Pyrenean Cavi Formation. This is tion of slates and quartzites, faulted against the above supported by the Caradoc faunas found in both areas. quoted high-grade rocks which form the oldest beds Also the conglomerates of Les Guilleries can be compared exposed in Les Guilleries. Towards the top, the sequence to the Rabassa Conglomerate of the Pyrenees. is again faulted, so that the top of the Ordovician and With respect to the correlation with the Montseny its stratigraphical contact with the Silurian cannot be massif, the faunas are similar in both areas (see Villas observed. The stratigraphical units seen in northwest- et al., 1987, for a discussion). However, the volcanic ern Montseny are not observed in Les GuiIIeries. Two sequence of Les Guilleries must be older than the fossiliferous localities have been found in the se- upper Ordovician beds described in the Montseny quence containing acid volcanic rocks (Durán 1985). massif,since these are the latest Ordovician beds found The faunas indicate a Caradoc or Caradoc to middle immediatelly below the Silurian, this part of the sequence being faulted out in Les Guilleries. Nevertheless, no some decades later by Puschmann (1968a, 1968b). A volcanic rocks have been reported up to now in the recent revision based upon new collected faunas of the Montseny massif in a lower stratigraphical position. Paleozoic area near Barcelona has allowed the recog- nition of severa1 graptolite zones (Julivert et al. 1985). Acid volcanic rocks are found once more to the The -atavus and -tumescens zones are respectively the south in the Serra de les Pedritxes (Durán et al. 1984, oldest and the youngest zones found. In addition, Ubach, 1990) where they are asssociated with a se- Greiling andpuschmann (1965) recognized the existence quence of slates and greywackes which in some local- of M.fritschi linearis ~oucxk,probably near the top of ities (near Olesa, for example) show abundant sole the black shales, in the transition to the next formation. marks. Slates and greywackes form the entire Paleo- The -atavus zone is the oldest zone recognized. The zoic outcrops which override the Tertiary beds of the lack of older faunas could be simply due to unfavour- Ebro Basin, between Les Pedritxes and Capellades, able environmental conditions. The existence of a although acid volcanic rocks are restricted to Les certain thickness of sediments between the Asghill Pedritxes. The sequence of the Serra de les Pedritxes faunas and the first occurrence of graptolites allows to can be tentatively correlated with the sequence with interpret the sequence as continuous. However, it acid volcanics of Les Guilleries, although there is no could also be that a small hiatus exists between the paleontological evidence to support this. In the Capellades Silurian and Ordovician, as is common in the Iberian area, a small limestone outcrop (Serra, 1989) could massif (Truyols and Julivert, 1983). re~resentthe Ashgill carbonate horizon. Although black shales are the most common rock Brachiopod faunas assigned to the Caradoc were type, the sporadic occurrence of other rocks coupled reported last century from severa1 localities from the with differences in the slates, allows the recognition of surroundings of Barcelona (Barrois, 1893; Almera, a certain lithostratigraphical succession (Fig. 4). The 1898). However, these localities have yielded, besides most striking lithologic variations, as observed in the brachiopods, a cystoid fauna (in Montcada, for exam- area near Barcelona, are: 1) the existence of chert ple) which can be better attributed to the Asghill layers and basic volcanic rocks and/or sills in the (Meléndez and Chauvel, 1981). The horizon contain- lower part of the sequence (Llandovery), 2) the exist- ing these faunas is probably the same carbonate horizon ence of interlayered thin quartzite beds in the middle referred to previously. Carbonate beds also crop out at part (Wenlock) of the Silurian sequence, 3) the exist- Collcerola (=Tibidabo massif), between Barcelona ence of black shales wjth sulphide layers and nodules and Molins de Rei. These beds are associated with (Wenlock or lower Ludlow), and 4) the existence of interlayered basic rocks (Gil-Ibarguchi and Julivert, thin limestone layers in the uppermost part, indicating 1988). The stratigraphic position of these carbonate the transition to the overlying La Creu Formation, beds is doubtful, however they are found near the although the contact is never clearly seen because of contact with the Silurian, also containing interlayered tectonisation, due to ductility contrast. basic rocks. For these reasons, the carbonates have been tentatively assigned to the Asghill (Julivert and The above succession is based upon the localities Durán, 1981). Also in this area a quartzite horizon is near Barcelona. Some of the features described can found, apparently at the contact with the Silurian also be found in other localities. The black shales with black shales. This horizon could be the equivalent of sulphides are found also in Malgrat and in Espluga de the Bar Quartzite in the Pyrenees, although no quartzites Francolí (Prades Mountains), which indicates that they have been found in the northern Montseny massif probably occur throughout the entire Catalonian Coastal where the contact with the Silurian is well exposed. Ranges. Also the part of the sequence with interlay- ered thin quartzite beds is found in the Montseny The remainder of the Ordovician sequence in Coll- massif, and is probably widespread. However, the cerola and the outcrops west of the Llobregat river basic rocks seem to be restricted to the area near consist mainly of slates, locally with silt laminae, and Barcelona or, if present in other areas, they are minor some interlayered quartzites, but no key horizon to in occurrence. correlate with the Ordovician sequences of other massifs has been found.
UPPER SILURIAN AND DEVONIAN CARBON- SILURIAN BLACK SHALES ATES The Silurian consists mostly of black shales or Above the black Silurian shales is a carbonate slates with abundant graptolite faunas. These faunas sequence which is best exposed at Santa Creu d'olorda, Ihave already been reported at the end of last century near Barcelona. The sequence can be divided into two (Barrois, 1983, 1901), and new collections were made formations. The lower part (La Creu Formation) is a the age to be essentially Pridoli, although the lower- most part is still Ludlow and the last few metres are Devonian (Lochkovian). The Olorda Formation has yielded a Lochkovian graptolite fauna (Greiling and Puschmann, 1965; Ju- livert et al. 1985) in its lower part (Member A), and dracrioconarids and conodonts in members B, C and D (Julivert et al. 1987). New collections of conodonts
Mat~lvenodular (S. Garcia-López) and dacrioconarids (M. Truyols- Massoni) have allowed the definition of the Lochko- vian, the Pragian and the Emsian. For a list of species and age discussion see Garcia-López et al. (1990) . The above formations are found throughout the Catalonian Coastal Ranges, although no detailed Pyrite -r~hlevel stratigraphical sequences have been described for other localities. The two formations can be recognized through q~arlzitebedl the lithological and fossil descriptions of previous authors, in the following localities: 1) Malgrat, where Almera (1913) reported the existence of ((tentacu-
Thin (1-5 cm) and lites>>(Olorda Fm.), as well as aOrthoceras>>lime- lhlck (up lo 15-20 cm) stones (La Creu Fm.), 2) Severa1 localities in Barce- LLANDOVERV occasionally lotming lona (Gracia, Montcada), where also ((Orthoceras>> horizonr up to 1-2 m thlck . and dolerlle limestones and (
Ousrlziles end slsles from the Olorda Formation, 5-6) northwest (Aiguafre- da-Avencó creek) and southw'est (Figaró) Montseny, where Pushmann (1968a, 1968b) described the two formations under the name of aorthoceraten Kalkens (=La Creu Fm.) and (
Figure 5.- Stratigraphic sequences of the lower part of the Carboniferous, according to Anadon et al. (1985), simplified. A, blackcherls (Tournaisian). B, carbonate horizon (Visean). C, lower part of the culm sequence. I, Limestones; 2, Chert with phosphate modules; 3, Conglomerates; 4, Pelites; 5, Culm sequence.
ern (Canoves) areas of the Montseny massif, El Montnegre, northern part of the ranges only thin to moderate thick several points near Barcelona (El Putxet, Santa Creu sequences have been preserved. d'olorda, Sant Bertomeu), El Papiol, and Gavi. A somewhat different succession is found in Hort- In all these localities (Fig. 5) the sequence starts by savinya (Montnegre), where directly overlying the a 10-20 m horizon of black chert with phosphate black cherts there is a mud-supported conglomerate, nodules. Above is a carbonatelshale horizon, some so that the shalellimestone horizon is missing. This is, 10-25 m thick. The carbonate content of this horizon is however, a local feature and can be interpreted as due variable. In Malgrat (El Montnegre) it forms a rather to erosion, the conglomerates representing the infi- homogeneous limestone level, whilst in Papiol it con- lling of a paleochannel. sists of an alternation of pink or purple shales with interlayered thin dolostone and limestone beds, and in Concerning the ages, the basal cherts have been El Montseny it forms a sequence of alternating lime- attributed to the Tournaisian, the shale and limestone stones and green shales (Anadón et al. 1985). horizon has yielded a fauna with Posidonomya becheri and Drevermaniapruvosti which indicates the Visean. These horizons are quite constant throughout the The overlying ccculm>>sequence must still be Visean northern part of the Catalonian Coastal Ranges. They for its lower part, whilst the age of its upper part are followed by a thick terrigenous succession (shales, depends on the thickness of the sequence preserved. In greywackes and conglomerates) with the sedimentary this respect, except in El Montnegre and western structures and trace fossils peculiar to tuibiditic se- Montseny, the thickness preserved is very small, and quences (culm facies, found throughout the Hercynian the ccculm>>sequence includes probably only the Visean. chain of Europe). In El Priorat (southern Catalonian Where a thick sequence exists, as in El Priorat, it Ranges) this terrigenous sequence reaches a thickness probably reaches the Westfalian, as in the Montalbán of about 2500 m (Anadón et al. 1985), but in the massif (Iberian Chain; Quarch, 1975). CONCLUSIONS AND COMPARISON WITH ALMERA, J., 1898: Compte-rendu de l'excursion du mercredi 5 NEIGHBOURING AREAS Octobre, i Gava, Begas et Vallirana. Bull. Soc. Géol.France, 26: 789-800. ALMERA, J., 1901: Zonas graptoliticas de Barcelona. Akten d. The Paleozoic stratigraphic succession in the Cata- funftenlnt. Kongr. Kathol. Gelehrten (Miinchen 1900): 413-414. lonian Coastal Ranges has strong similarities with ANADON, P., JULIVERT, M. and SAEZ, A., 1985: Aportación al those of Central and Eastern Pyrenees, and differs conocimiento del Carbonifero de las Cadenas Costeras Catala- remarkably from those of the Iberian massif and the nas. C. R. Xdme Congr. Internat. Strat. Géol. Carbon. (Madrid Iberian Chain. 1983), 1: 99-106. ASHAUER, H.and TEICHMULLER, R., 1935: Die variszische und The pre-Caradoc sequence can in broad terms be alpidische gebirgbildung Kataloniens. Abh. Ges. Wiss. Gott. correlated with the Jujols and Canavelles formations math.-phys. Kl.. 3: 1-79. of Central Pyrenees, and like in the Pyrenees it has not BARROIS, Ch., 1893: Observaciones sobre el terreno Silurico de yielded any fauna. Also, as in the Pyrenees, ortho- 10s alrededores de Barcelona. Bol. Com. Map. Geol. España, 19: gneiss bodies probably representing Late Precambrian 245-260. or/and Late Precambrian-Early Cambrian intrusions BARROIS, Ch., 1901: Note sur les graptolites de la Catalogne et (but still subject to controversy), are found at or near leurs rélations avec les étages graptolitiques de la France. Bull. the base of the sequence. Soc. Géol. Fr., 1: 637-648. CAVET, P., 1957: Le Paléozoi'que de la zone axiale des Pyrénees The Caradoc-Ashgill is similar in facies and faunas orientales fran~aisesentre le Roussillon et 1'Andorre. Bull. between the Catalonian Coastal Ranges, the Pyrenees, Serv. Carte Géol. France, 254 (55): 303-518. and also in Sardinia and other Paleozoic massifs around DURAN, H., 1985: El Paleozoico de Les Guilleries. Unpublished the western Mediterranean, although in the Catalonian Ph. D. Thesis Univ. Autónoma de Barcelona: 1-243. Coastal Ranges the sequence seems to be thicker. One DURAN, H., 1990: El Paleozoico de Les Guilleries. Acta Geol. peculiarity of the Caradoc sequence is the existence of Hispdnica, 25(1/2): 83-103. a major acid volcanic event. DURAN, H., GIL IBARGUCHI, J.I., JULIVERT, M. and UBACH, The Silurian consists mainly of its characteristic J., 1984: Early paleozoic acid volcanism in the Catalonian Coastal Ranges (NW Mediterranean). In: F.P. Sassi and Julivert black graptolitic shales, so widespread throughout Eds., IGCP S, Newsletter 6: 33-43. western Europe, and do not shows any peculiarity worth noting. FAURA SANS, M., 1913: Síntesis estratigráfica de 10s terrenos primarios de Cataluña, con una descripción de 10s yacimientos The Devonian (and uppermost Silurian) forms a fosiliferos mis importantes. Mem. R. Soc. Hist. Nat., 9 (1): 1- sequence of marls and limestones with an abundance 202. of conodonts and dacrioconarids and a paucity of GARCÍA-L~PEZ,S., JULIVERT, M., SOLDEVILA, J., TRUYOLS- benthonic faunas. Although with some peculiarities, MASSONI. M. and ZAMARREÑO, I., 1990: Biostratigrafia y Facies de la sucesión carbonatada del Sillirico Superior y Devónico the Devonian facies in the Catalonian Coastal Ranges Inferior de Santa Creu d'Olorda (Cadenas Costeras Catalanas, are similar to those of the Pyrenees, Sardinia, and NE de España), Acta Geol. Hispdnica, 25(1/2): 141-168. other Paleozoic areas of the Western Mediterranean, GIL-IBARGUCHI, J. I., and JULIVERT, M., 1988: Petrologia de la whilst they llave no equivalent in the Iberian massif,the aureola metamórfica de la granodiorita de Barcelona en la Sierra only exception being the Pisuerga-Carrión Province, de Collcerola (Tibidabo). Estudios Geol., 44: 353-374. of the Cantabrian zone. GREILING, L. and PUSCHMANN, H., 1965: Die Wende Silurianl Devon arn St. Creu d'Olorde bei Barcelona (Katalonien). Senckenberg. The Carboniferous is characterized by its thick lethaea, 45: 453-457. < MELENDEZ, B.and CHAUVEL, J., 1981: Sur quelques Cystoi'dées SIJP, J. W. C. M. VAN DER, 1951: Petrography and geology of cités par les Drs. J. Almera et M. Faura dans l'ordovicien de Montseny-Guilleries (NE Spain). Tesis Univ. Utrecht: 1-99. Barcelona. Acta Geol. Hispanica, 14: 318-321. UBACH, J., 1990: Geologia de 10s materiales paleozoicos de las PUSCHMANN, H. 1968a: Stratigraphische Untersuchungen in escamas de la Cordillera Prelitoral Catalana al Este del rio Palaozoikumder Montseny (Katalonienlspanien). Geol.Rundschau, Llobregat. Acta Geol. Hispanica, 25(1/2): 113-121. 57 (3): 1006-1088. PUSCHMANN, H. 1968b: La série paléozoi'que du massif du Mont- VIDAL, L.M., 1886: Reseña geológica y minera de la provincia de seny (Catalogne, Espagne du Nord-Est). C.R. AC.SC. Paris, 266: Gerona. Bol. Com. Map. Geol. Esp., 13: 209-380. 657-659. 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