Comunicacoes Geologicas, 2007, t. 94, pp. 53-79
Devonian and Carboniferous palynostratigraphy ofthe South Portuguese Zone, Portugal - An overview.
Z. PEREIRA*, 1. MATOS**, P. FERNANDES*** & J. T. OLIVEIRA****
Keywords: Devonian, Carboniferous, Palynostratigraphy, South Portuguese Zone.
Abstract: The South Portuguese Zone (SPZ) represents the southern branch of the Iberian Variscides and comprehends the following geologic domains: the Pulo do Lobo Antiform, the Iberian Pyrite Belt, the Baixo Alentejo Flysch Group and the Southwest Portugal (Aljezur and Bordeira Anticlines). An overview ofall the results recently achieved in palynostratigraphic research ofselected sections all over the SPZ is presented. A chronostratigraphic correlation of the stratigraphic units recognized across the ZPZ and its geodynamic and palaeogeographic implications is attempted.
Palavras-chave: Devonico, Carbonifero, Palinostratigrafia, Zona Sui Portuguesa.
Resumo: A Zona Sui Portuguesa (ZSP) representa 0 ramo sui do Orogeno Varisco Iberico e compreende os seguintes dominios, de norte para sui: 0 Antiforma do Pulo do Lobo, a Faixa Piritosa Iberica, 0 Grupo do Flysch do Baixo Alentejo e 0 Sector Sudoeste (Anticlinais da Bordeira e Aljezur). No presente trabalho apresenta-se uma sintese dos conhecimentos palinoestratigraficos obtidos em seccoes seleccionadas dos varios dominios da ZSP. Os dados obtidos permitem estabelecer correlacoes cronoestratigraficas em toda a Zona Sui Portuguesa, contribuindo assim para 0 melhor conhecimento da sua evolucao paleogeografica e geodinamica.
1. INTRODUCTION shallow siliciclastic sea that underwent crustal extention during the late Devonian (Strunian) and the lower The South Portuguese Zone (SPZ) represents the Carboniferous giving rise to an impressive bimodal southern branch ofthe Iberian Variscides (Figure 1). It is volcanism. Related with this volcanism near 90 massive almost entirely composed of Upper Palaeozoic sedimen sulphide deposits were formed. The Baixo Alentejo tary rocks of late Devonian to the Moscovian (Late Flysch Group (BAFG) is composed of southwestward Carboniferous) age. The following geological domains prograding sandy turbidites ofLate Visean to Moscovian are recognized in the SPZ (OLIVEIRA, 1990): the Pulo do age that filled a foreland basin. Finally, the Southwest Lobo Antiform, the Iberian Pyrite Belt, the Baixo Portugal Sector (SWPS) still part of the siliciclastic sea Alentejo Flysch Group and the Southwest Portugal during the late Devonian, evolved to a distal carbo (Bordeira and Aljezur Anticlines). nate/shale platform that only during the Moscovian The boundary between the Pulo do Lobo Antiform became part of the Variscan orogeny. and the Ossa Morena Zone, a major shear zone, is in The rock succession ofthe SPZ attracted researchers, several places underlined by the Beja-Acebuches particularly exploration companies, because of its famous Ophiolite, a remnant of an oceanic realm closure. The IPB polymetallic massive sulphides ore deposits (e.g., Pulo do Lobo Antiform is currently interpreted as a the world class Neves Corvo deposit). Geological research Variscan palaeo-accretionary prism (OLIVEIRA, 1990). was mainly concentrated on lithostratigraphy, petrology The Iberian Pyrite Belt (IPB) was part ofa late Devonian and geochemistry. More recently, biostratigraphy, sedi-
* LNEG-LGM, Rua da Amieira, 4465-965 S. Mamede lnfesta, Portugal ([email protected]). ** LNEG-LGM, Rua Frei Amador Arrais 3, Ap.104, 7801-902 Beja, Portugal. *** ICIMA, Centro de Investigacao Marinha e Arnbiental, Universidade do Algarve, 8005-139, Faro, Portugal. **** LNEG-LGM, Estrada Portela, Zambujal Alfragide, Ap.7586 , 2720-866 Amadora, Portugal.
© INETI 2007. Todos os direitos reservados . 54 Z. PEREIRA, J. MATOS, P. FER NAN DES & J. T. OLI VEIRA
A N
ATLANTI C OCEAN
38'
FARO '" 9' 8'
Pyrite Belt Sado Basin o pos-mesozctc cover [: '"is. :j Volca no Sed imentary Comp lex ",- Volcano Sedimentary Complex o Sines and Mon ch iqu e Mesoz oic Ma ssifs CVS in bore holes: I::PO:1 Phylli t e Quart:nte Group o Volcan ics E =~~~1I nd i f e r enc i a t ed Mesozo ic rndtteren ctated Pateeozotc sedim ents (Upper sae c Basin} Pula do Lobo AntUorm Baix o Alen tejo flysch Gro up E::::~=i Charu;a Groop FauLt, norma l fa ult • Brej eira Formation T hrust EiF7- ~ Fe rretre -Ftc etbo Group Mira Formation Village Ift'.,:1 ~ nl · Pula do Lobo Oceanic Sediments o . Borehole . studied bore hole J and MORB basalts (-, t g1~~a Mert ola fo rmati on
SW Port ugal 0IIIIIl Alj ez ur and Borde ira Anticlines
Fig. I- Geological sketch map of the South Portuguese Zone (adapted after OLI VEI RA , 1990; Geological Map of Portugal 1/500000, Oliveira et al. 1996). Devonian and Carboniferous palynostratigraphy ofthe South Portuguese Zone, Portugal - An overview 55 mentary geology, physical volcanism and sediment OWENS et al., 2004 ; STREEL et al., 1987; STREEL, 1996). geochemistry deserved more attention and are now The choice ofalternative schemes was stated by the presence current fields of research. of very consistent local miospore assemblages in South Palynological studies of the SPZ extend back to Portugal. The defined zonal taxa used for the latest 1980s. Palynostratigraphy was for the first time tested in Devonian and Carboniferous of the South Portuguese sev eral units of the SPZ as part of a mapping pro Zone are presented in Figure 2. Stratigraphically impor gramme carried out by the Portuguese .Geological tant and typical taxa are illustrated in Plates I and II. Survey (OLIVEIRA et al., 1986; CUNHA & OLIVEIRA, 1989). At that time palynostratigraphic work was also undertaken in the Spanish sector of the Pulo do Lobo 3. GEOLOGICAL SETTING Antiform (GIESEet al., 1988; LAKE, 1991). In the following AND PALYNOSTRATIGRAPHIC years more focussed projects on the biostratigraphy were FRAMEWORK OF SPZ developed. Palynostratigraphy represents the best tool to date the This section deals with the stratigraphic palynology SPZ lithostratigraphic units, allowing reliable stratigraphic ofall sections, boreholes and spot samples studied by the correlations across the basins and giving support to struc authors. Description of the new palynological data is tural, palaeogeographic and geodynamic interpretations. .presented here. In case ofpreviously published data only This paper presents an overview of all results recently a brief review is presented. achieved in palynostratigraphic research of selected sections all over the SPZ. The palynology data has allowed the establi shment of the general chronostratigraphic 3.1. Pulo do Lobo Antiform correlation chart for all the domain s ofthe SPZ (Figure 2). The Pulo do Lobo Domain is an antiformal structure located in the northern part ofthe SPZ, wher it is in direct 2. METHODS contact with the Ossa Morena Zone (OMZ). In the core of the structure crops out the Pulo do Lobo Fm. and is The studied samples were collected in complete compo sed of phyllites , quartzites, minor felsic volcanics outcrop sections, boreholes and occasionally spot and amphibolites (former basalts) with MORB-type samples. In the IPB, where a large number of boreholes geochemical affinity at the lower part (MUNHA, 1983; are available, drilled by mining and exploration compa EDEN, 1991; QUESADAet al., 1994). nies and by the Portuguese Geological Survey. Samples In the north limb ofthe structure, the Ferreira-Ficalho Were preferably collected from cores and in a few cases Group (Figure 3) includes from base to top the following sample s were also collected from the mine addits (e.g., units (CARVALHO et al., 1976; OLI VEIRA et al., 1986; Neves Corvo and Aljustrel). In the SW Sector samples GIE SE et al., 1988; OLIVEIRA, 1990; EDEN, 1991 ; were mainly collected along the costal sections of the QUESADA et al., 1994): the Ribeira de Limas Fm. is area. compo sed ofphyllites, quartzwakes and minor intercala Biostratigraphic research is based on palynomorphs tions of tuffites with a tectonic deformation similar to and standard palynological laboratory procedures were that of the Pulo do Lobo Fm.; the Santa Iria Fm. is made employed in the extraction and conc entration of the up of greywackes, siltstones and shales, forming a palynomorphs from the host sediments (WOOD et al., flysch-like succession; and the Horta da Torre Fm. is 1996). The slides were examined with transmitted light, compo sed of dark shales, impure sandstones, siltstones per BX40 Olympus micro scope equipped with an and quartzite beds with strong bioturbation. The Santa Olympu s C5050 digital camera facility. All sample s, Iria and Horta da Torre Fms. are affected by a main fold residues and slides are stored in the Geolo gical Survey of ing phase with associated cleavage. The group thickness Portugal (LNE G - LGM). The miospore biozonal is unknow, but estimated at 500 m. scheme used follows the standard Western Europe The south limb of the structure is represented by the Mio spore Zon ations (after : CLAYTON et al. , 1977; Chanca Group (Figure 3), which comprises the following CLAYTON 1996; CLAYTON et al., 2003; HIGGS et al., 1988; units (PFEFFERKORN, 1968; SILVA, 1989; CUNHA & HIGGS et al., 2000 ; MAZIANE et al., 2002 ; OWENS, 1996; OLI VEIRA, 1989; OLI VEIRA, 1990; SILVA et al., 1990): the Bio str at ig ra p hy Vl Cro nostr a ti gr a p hy Pa ly nologlc,,1e ve nts So ut h Port ug ue se Zo ne (SP Z) 0\ Gonlatit e s Mi o spo re s
Fa u ll har b on. SWSP W.Eu rop" Portu. "l Portugal Pulo do Lobo Antiform I Regional GrobillISt",,,, Port". ..1 pyrlt"e"lt BAFG SW PS ! W.E " rop" " n St "g.. (Korn. 19911 e iozones (l ) 81010n ".(21 lnd.." sp"d"s(:i) FFGroup GCGroup
Ka si m o vian ST ...... Stepha nia n
-----_._- ---~ ~ O T OT Th ymospo r a p 5e vdolhiessen;; First a p pearance o f Th ym osporo sp p.
Mo scovll.., Rol strickict oculeoto C SL SL Torlsp ora ~'ecuris First appearance 01 romoora Br"J"I,.. Fm. I-- NJ NJ Florinlte 5 j u nior Westphalian B SrejelraFm I--
RA RA Ro di iz onotes a ligerens A First a p pearance of R. al ifjerens tocreese in La eVif/a lo sp o rlt('s a nd C. Gos trlaceras o ng us tum G2 S5 SS Cirratr lradites sa turn! sa tu rn i Gas l rlrx:(', as /ist e,,' Bolshklrla n G lb ovcuoonetes prob iretlcu /at us FR FR G" ConcefiocerQSSPP Reticu /a t lsp orltes reticuiatus R2, Bi lm ult es me tobllin u is r--" ----:- Namurian (Upp er ) R2b M o " an acero hes er iurn Bilin ult l!J ra cili s KV KV R" Cro ssJsporo ko sa nke i ~ RI , Ret lc ul o ceras re rlcu /a rum Rio Va lMes ku llman ni f4-- Appea, a nc.e o f R einJch~sporo a nd Mir"'m. /Qu..brad u Fm. ~ inc.re a s. o n C. kosonkel s SO Se rp uk ov illo n Namur ian (lower ) TK
? Exti nc tio n at R. ni gra . G. so m oeo NC NC pos trlotum Zon e Be ll/spores r ntidus 1"'-- Rotasp o r a ap p. lind C. mo cu tosa roctns Zone VF SN' Savitrisporite:; nux" Molrtol. Fm. Men olaF m. s 1111 er Zone First a p pearance of S.nu x eren ist ia Zo ne NM ea tstrtckia nigra" hudson; Zo ne N,' fi rst ap peara nce o f R, ni gra Vise a n Vise an 1--' M u,r a ~ J oF m . TC
TS TS Kn oi/ ispo"res st ep h a ne ph oru s vsc PE PU PU ivcos ooro p usillo
f irst appe arance of L. pu sl/lo CM CM Schopf ltes cto vtqer l acun.. PC PC Spelaeotrllet es pr et io sus fir st aPpearanc.!!!o f S. p re tio sus r c umauta n 'rournatsta n BP BP Sp r lae o tr il e tes bolteotus L;lcunl! G. Sord.l .t. Fm. HD HD Cr/s to tispori res hibernicus
V, V, Vollo t isp or i res ver rucos u s LN LN v er rv co stsoornes nltid us r----- h t int lon of R. lep ld ophyro T"", ,,n. , Fm. Wo LE LE tnaoutroanes exotonotus
LL LL Ret isp o ro tep idc p tw ta PQ Grou p t'J -e I VH VH Gr an d /sp oro ec hino to S.lrla/H .Torr" Fm. lI..pr.u Fm. m VCo First appearanc e of G. ec hlno to ;0 fa m e nni an Fame n ni an VCo Gro nd isporo cornu to ~ rn I vc» First appe a ran c.e of G. cv rnu to ~ G' :- GH s:: V ~ o E la cun" la cu n.. , Y' Db ~ D. "'r1 Cb m C. ;0 Bb Z fr a sni a n f ra sn ia n » B. z A o BM BM La hOl onoUile tes media ~ i ;_ ' m . G. fo Fm. PQ G,oup I S~in l rn V> BJ B' Venuco slsporJres bulli/e rus ? PUIOdo lobo/A1.o1"i.Fm., Ro Too reo .... o Fig. 2 - Latest Devonian and Carboniferous of SPZ. (I. Western European Miospore Zonation (CLAYTONet al., 1977; CLAYTON 1996; CLAYTONet al., 2003, HIGGS et al., 1988; HIGGS et aI., "r- <: 2000; MAZIANE et al., 1999; OWENS, 1996; OWENSet aI., 2004; STREEL et al., 1987; STREEL, 1996); 2. South Portugal miospore Zonation (PEREIRA, 1999); 3. Defined guide taxa used rn ;; for the latest Devonian and Carboniferous of the South Portuguese Zone (PEREIRA et al., 2007; Present work)). » Devonian and Carbon iferous pa lvnostratigrophy ofthe South Portuguese Zone, Portugal -An overview 57
Atalaia f m. composed mostly ofphyllites and quartzites, PEREIRA et al., 2006a, b) as an accretionary prism related sharing with the Pulo do Lobo Fm. the same type of to a northward dipping subduction (SILVA et aI., 1990; tectonic deformation; the Gafo Fm. made up of a thick QUESADA et al., 1994, SILVA, 1998) and as a suspect pile of greyw ackes siltstones and shales forming a flysch terrain (RIBEIRO et aI., 1990). succession, with intercalations and intrusions of felsic and mafic volcanics showing two main episodes ofNW trending folds and related cleavages; and the Represa 3.1.1. Pulo do Lobo palynostratigraphy Fm. which is composed of siliceous siltstones, shales, greywackes and minor intercalations of fine volcano The Pulo do Lobo Antiform units were recently genic sediments. The group thickness is estimated at investigated for palynostratigraphy (PEREIRA et al., 2006, 1100 m. Figure 2, 3). No age determinations were achieved for The overall structure has been interpreted as an anti the Pulo do Lobo and Atalaia Fms., probably due to the cline (SCHERMERHORN, 1971; CARVALHO et aI., 1976; high grade of metamorphism that affected these units, OLIVEIRA et al., 2006; PEREIRA & OLIVEIRA, 2006; however the sequence is older than early.Frasnian. The
A N
Sampled Places t93 sempte studie s}
PULO DO LOBO ANTICLINE
Ferreira-Ficalho Group Gato Group HortadaIorre/St"lriaFormations Represa Formation (Late Famennian age) (Late Famennian age)
[/r>p,j Ribeira de Limas Formation ~ Galo Formation ?' (Early Frasnian age) •~ (Early Frasnian age)
Pulo do Lobo! Atalaia Formations
PYRITE BELT
Mertola Formation (Visean age)
Volcano·sedimentary Complex I v ~} j (Late Famennian -Visean age)
Phillito-Quartz itic Formation I POl (Early Frasnian-Strunntan age)
Fig. 3 - The Pulo do Lobo Geology (and studied localities) . 58 Z . PE REIRA, J. M ATOS, P. F ERNANDES & J. T. O LIVEIRA
Ribeira de Limas and Gafo Fms. revealed the presence of and shales with intercalations of limestone lenses and moderately preserved miospore assemblages assigned to nodules at the upper part of this unit, which as a whole the BM Biozone of lower Frasnian age. The assemblage were laid down in a marine siliciclastic platform. The includes An eurospo ra greggsii, Chelinospora concinna , thickness is in excess of 200m (base not known). The Cristatisporites triangulatus, Cristatisporites sp. cf. C. VSC is dated as late Devonian to late Visean age princi inusitatus, Cymbosporites sp., Emphanisporites rotatus, pally on palynomorphs and rare conodonts (OLIV EIRA , Geminospora lemurata, Loph ozonotriletes sp., Verruco 1990; OLIVEI RA et aI., 1997, OLIVEIRA et aI., 2004; sisporites bulliferus, V premnus and V scurrus. All PEREI RA et aI., 2004). The VSC incorporates several samples contain rare acritarchs and prasinophytes. episodes of intrusive and extrusive volcanism, with The Santa Iria, Horta da Torre and Represa Fms. dominant rhyolites, dacites, basalts and minor andesites, yie lded well-pres erv ed asse mblages of miospores and intercalations of black shales, siltstones, minor assigne d to the VH Biozone of late Famennian age quatzwackes, siliceous shales, jaspers and cherts and a (PEREIRA et al., 2006 a,b). The assemblages Include abun purple shale member at the upper part of the complex. dant Grandispora echinata which indicates the base of The thickness is variable, from few tens of meters to the biozone , together with Ancyrospora sp., Ancyros more than 1000m. The VSC was laid down in a deep pora? imp licata, Apiculiretusispora sp., Aurorasp ora submarine environment. macra, Cristicavatisp ora dispersa, Diducites versabilis, Regionally the belt is .divided into two branches D. poljessicus, Emphanisporites annulatus, Grandispo ra (OLI VE IRA, 1990): the North and the South branch cornuta, G. famenensis, G. gracilis, Plicatispora sp., (Figure 4).The North branch extends from Palma Punctatisporites spp., Retusotriletes p lanus, R. triangu (Alcacer do Sal), below the Cenozoic sediments of the latus, R. rugulatus, Rugospora explicata, R. radiata and Sado Basin (at the west), to Mina de Sao Domingos mine Teichertospora iberica. All samples contain very rich (at the east) (VOLIVEIRA et aI., 1998a, b; MATOS et aI. , assemblages of acritarchs and prasinophytes. 1998, 2000, 2003). This branch incorp orates both The early Frasnian and late Famennian ages of the autochthon sections, where it is possible to identify the Ribeira de Limas/Gafo sequence and Santa Iria-Horta da VSC sequence overlain by the Freixia l Fm. turbidites, Torre/Represa sequences indicate they are separated of and allochthon sections composed of several tecton ic about 14 My. This fact reinforces previous structural sheets that include PQG sediments and VSC volcanics interpretations that suggested the existence of an uncon and sediments. The South branch refers to the rooted formity between the Santa Iria/Horta da Torre Fms. and anticlines and extends from the Pornarao Anticline (west the underlying Ribeira de Limas Fm.. termination ofthe Puebla de Guzman Anticline in Spain) The stratigraphic correlations of these units of both through the Neves Corvo-Rosario Anticline to the Lousal limb s of this antiform suggests that these were part of region (Figure 4). Conform ably above the VSC is a the same sedimentary basin that appears to have been turbidite succession, known as Mertola Fm. which is the superimposed over an acretionary prism, now preserved lower unit of the Baixo Alentejo Flysch Group (BAFG). in the Pulo do Lobo/Atal aia Fm. (PERE IRA et al., 2006a,b). 3.2.1. Iberian Pyrite Belt pal ynostratigraphy
3.2. Iberian Pyrite Belt The selected lithostratigraph ic sections investigated for palynostratigraph ic purposes are depicted in Figure 4. In general terms, the stratigraphy ofthe Iberian Pyrite In the North branch three sections were studied, i.e., Belt (Figure 4) consists of two major units, the Phyllite Alber noa, Serra Branca and Mina de Sao Domingos. Quartzite Group (PQG) and the Volcanic-Sedimentary The palynomorph assemblages were recovered mostly Complex (VSC). The PQG is dated as late Devonian age from drill cores, compl emented with outcrop samples. by ammonoids, conodonts and palynomorphs (BOOGAARD, Within the autochthon successio ns, moderately preser 1967, FANTI NET et aI., 1976; CUNHA & O LI VEI RA, 1989; ved miospore assemblages were identified in shales OLI VEIRA et al., 1997; O LI VEI RA et al., 2004, PEREI RA et interbedded in the lower part of the VSC and doubtly in aI., 2004). The PQG forms the detritic basement and is shales of the PQG (Albem6a) . These assemblages are compo sed mostly of phyllites, quartzites, quartzwackes assigned to the VCo and VH Bizones of late Famenni an PYRITE BELT ~ NORTH BRANCH '"tr Albernoa Serra Branea Sllo Domingos l:l '"l:>. Q (Grand/sporo "'hinate) v H 8 ~
'-;;;.;t (Rairtrickia nigra) Nl !Grondispcro echinate)VH(;j· '"Cl 1:; '2 '2"' 0;> PUILycospora pusillal Cenozoic sediments '" PU(Lycospcro pus/llo ) ~ Shales andgreywackes (Flysch) ~. -E;: VH(Grand/spatoechinate) .g Shales, siltitesandgreywackes ~ 8 veo lGrondisporo cornuta) ~ VHIGrondispora echinate) ;;,. Tufites, volcanoclastics ~'" 'am Purple shales (bv) ;;,.'" ~ Jaspes 0);Cherts (Ch) SOUTH BRANCH ~ ~ ~ Massif sulphides; Pyrite (Py) '"~ Lousal Cereal Neves Corvo Pomarllo Acid Volcanics '" Azinheira de Barros '"~ ~ Basic volcanics (spilites) ~ SOOm I 6; Nt {Raistrickia rJigra) :>.. • Diabases '" Limestones I· Shales andquartzites
Arenites( grevwackes, quartzowackes andquartzites)
Miospores
~ e: ) VH(Grandisp -0VH(GraM/spora echinata) IN(Verrucosisporites nitidusl Goniatites Fig. 4 - Synthetic stratigraphic columns selected from the Pyrite Belt (adapt. OLIVEIRA et aI., 2006). Vl \0 60 Z. P EREIRA, J. M ATOS, P. FE RNANDES & J. T. O LI VEIRA age. The VCo assemblage contain the zonal species Apiculiretusispora sp., Auroraspora sp., A. solisorta, Grandispora cornuta and Auroraspora sp., Diducites Crassispora sp., Cristatisporites triangulatus, Cristicava spp., Emphanispo rites rotatus, Geminospo ra lemurata, tispora dispersa, Cymbosporites sp., Diducites poljessi Punctatisporites sp., Retusotriletes planus, R. rugulatus cus, D. versabilis, Emph anisporites annulatus, E. rotatus, and Rugospora radiata. The VH assemblage is defined by Geniinospo ra Ietnurata , Grandispora cornuta, Punctatis the presence ofthe key specie, Grandispora echinata and porites irasus, Retusotriletes sp., R. crass us, Rugospora includes the taxa Auroraspora sp., Diducites poljessicus, explicata, R. radiata and Spe laeotriletes sp.. All samples D. versabilis, Emphanisporites rotatus, Geminospora enclose very rich assemblages of acritarchs and prasino lemurata, Grandispora corn uta, Punctatisporites sp., phytes. The fact that the autochthon and the allochthon Retusotriletes ph illipsii, R. planus, R. triangulatus, both have VH assemblages with strong similarities Rugospora explicata and R. radiata. All assemblages implies that were part ofthe same palaeogeographic realm. contain abundant acritarchs and prasinophytes. In the South branch research has been concentrated Higher in the VSC, palynomorph . assemblages in the Pornarao anticline, Neves Corvo mine and obtained from black shales are assigned to the Pu Biozone Lousal regions, and very recently in the Cereal anticline and comprises the zonal species Lycospora pusilla in asso (Figure 4). ciation with Auroraspora macra , Convolutispora sp., The most complete palynostratigraphic study unde r Densosporites sp., D. spitsbergensis, D. brevispinosum , taken in the Portuguese sector of the Iberian Pyrite Belt Dictyotriletes castaneaeformis, Discernisporites micro was the investigation of the Neves Corvo mine succes manifestus, Knoxisporites cf. triradiatus, Vallatispo rites sion . All the local rock units were accurately dated, and pusillites, V galearis, V verrucosus. so concluded a long standing stratigraphic controversy At the top of the autochthon grey shales, siltstones and providing a major contribution to the interpretation and thin bedded greywackes of the Freixial Fm. yielded of the local tectonic structure and ore genesis (OLIVEIRA moderately preserved miospores of the NM Biozone of et al., 1997; PEREI RA et al., 2001 ; PEREIRA et al., 2004 ; mid late Visean. The NM biozone assemblage is defined OLI VEIRA et al., 2004). This study allowed the following by the presence of the zonal specie Raistrickia nigra and main conclusions: abundant taxa such as Ahre nsosporites sp., Anaplanis porites sp., Crassisp ora trychera , Densosporites sp., ( I) The age of the PQG is late Famennian based on D. brevispinosunt, D. intermedius, Knoxisporites trira moderately to well preserved miospore assemblages diatus, Leiotriletes tutnidus, Ly cosp ora pusilla, assigned to the VCo and VH Miospore Biozones. The Microreticulatisporites sp., Va llatisporites vallatus and VCo Biozone assemblage includes the type speci es Waltzispora sp. In Serra Branca the NM assemblage Gra ndispora cornuta and abundant specimens of recovered from the Freixial Fm. also containes taxa such Auroraspora macra, Cris tatisporites triangulatus, as Emphanisporites rotatus, Geminospora sp., Retispora Diducites versabilis, D. poljessicus, Emphanisp orites lepidophyta, Rugospora radiata and Vallatisporites annulatus, Geminospora lemurata, Retusotriletes planus, verrucosus, which are interpreted as reworked miospores R. triangulatus, R. rugulatus and Rugospora radiata. of late Famennian age. Reworked Frasnian mio spores (Cr istatisporites sp., In the allochthon, shale s ascribed to the PQG yielded Contagisporites optivus, Aneurospora greggsii, Verruco a moderately to well preserved miospore LN Biozonal sisporites premnus and V scurrusi are well represented asse mblage (Mina de Sao Domingos section) that in the VCo studied assembl ages. The VH Biozone is contains Verrucosisporites nitidus, the index species in marked by the abundant presence of Grandispora echi assoc iation with the taxa Crassispora sp., Densosporites nata together with Ancyrospora sp., Auroraspo ra macra , sp it s bergensis, Geminospora lemurata, G. spongiata, Cristatisp orites tria ngulatus , Grandispo ra corn uta, Punctatisporites sp., Retispora lepidophyt a, Rugospora Emp hanisporites annulatus, Gemi nospora lemurata, radiata and Va llatisporites sp. with some rare acritarchs Retusotriletes planu s, R. triangulat us, Raist rickia and prasinophytes. Shales of the Represa Fm. contain variabilis, Rugospora radiata, Spelaeotriletes sp. and well preserved miospore assemblages assignable to the Va llatisporites pusillites. Acritarchs and prasinophytes VBBiozone. The assemblages contain Grandispo ra echi are well represented in the assemblages . Reworked nata the key specie, together with the taxa Ancyrospora Fras nian miospores are also documented in the VB sp., Ancyrospora? implicata, Aneurospora greggsii, assemblages; Devonian and Carboniferous pa lynostratigraphy ofthe South Portuguese Zone, Portugal - An overview 61 (2) The age of the VSC ranges from the late Strunian characterized by the first occurrence. of Bellispores to early late Visean. The LN, TS and NL Miospore nitidus together with abundant species of Crassispora Biozones are identified. The LN Biozone is marked by maculosa, Convolutispora venusta , Diatomozonotriletes the presence of well preserved and abundant specimens sp., Dictyotriletes sp., Leiotriletes tumidus, Rotaspora of Auroraspora macra, Densosporites sp itsbergensis, Facta and Savitrisporites nux. In the entire studied NC Geminospora sp ongiata, Grandispora corn uta, G. echi asse mblages reworked Strunian and Toumaisian nata , Knoxisporites literatus, Leiotriletes stru niensis, miospores are common. The Mertola Fm. also yielded Retispora lepidophyta, Retusotriletes incohatus, Rugos the goniatites Goniatites hudsoni and G? globostriatus of pora radiata, Tumulispora malevkensis, Vallatisporites late Visean A age and Arnsbergites arnsbergensis, pusillites and Vallatisporites verrucosus together with Arnsbergites falcatus and Hibernicoceras, which indi the index species Verrucosispo rites niditus. Rare speci cate the late Visean B confirming the results provided by men s of Aratrisp orites saharae nsis also occur. the palynomorphs in the Neves Corvo mine region Acritarchs and prasinophytes are very common in the (Olive ira et aI., 2004); assemblage. The TS Biozone is defined by the presence (4) Three stratigraphic hiatuses are recognized, of the key species Knoxisporites triradiatus and K. embracing the early to middle Strunian, the Toumaisian stephanephorus. Other taxa present include Anapicula and the early Visean. These hiatuses appear related to a tisporites sp., Convolutispora nigrata, Densosporites southw estward progressive unconformity; rarispinosus, Diatomozonotriletes sp., Dictyotriletes propius , Hym enozonotriletes caperatus, Knoxisporites (5) Precision of the biostratigraphic dating of the hederatus, Microreticulatisporites concavus, Propris massive sulphide orebodies that are intercalated in latest porites sp., Spelaeotriletes pretiosus, S. arenace us, Famennian (late Strunian) black shales. These age deter Vallatisporites pusillites and V. galearis. Reworked minations proved that all of the lithostratigraphic units Toumai sian palynomorphs are present. The NL Biozone, are involved in a pile of tectonic sheets (Figure 4). a local biozone defined by the fist occurrence of Raistrickia nigra (see the details described in the SSP The Pomarao anticline expos es a complete lithos below). Other taxa include Convolutisp ora sp., tratigraphic section of the Portugueses Pyrite Belt Densosporites rarispinosus, D. annulatus , Diatomo (Figure 4). Here, only shales of the lower part of the zonotriletes sp., Knoxisporites hederatus, K. triradiatus, sequence (Nascedios Member of the PQG) yielded K. stephanephorus, Leiotriletes sp., Lycospora pusilla, miospores assigned the LL Biozone of late Strunian age Microreticulatisporites concavus, Proprisporites sp. and (OLI VEIRA et al., 2006). Assemblage comprises mode Vallatisporites ciliaris; rately preserved specimens ofAuroraspora sp., Diducites sp., Emphanisporites rotatus, Knoxisporites literatus, (3) The Mertola Fm. flysch sediments yielded poorly Retispora lepidophyta and Retusotriletes sp., rare acri to moderately preserved miospores assemblages assigna tarchs and prasinophytes are also present. The overlying ble to the Biozones NL, SN and NC Miospore Biozones VSC is composed of three volcanic episodes and of the late Visean. The NL Biozone includes the guide interbedded sediments. Until now no biostratigraphic age species Raistrickia nigra and also common specimens of was obtained for VSC succession . Densosporites rarispinosus, D. annulatus, Diatomo In the LousallAzinheira de Barros/Mina da zonotriletes sp., Knoxisporites hederatus, K. triradiatus, Cavcira region the Pyrite Belt develops complex antifor K. stephanephorus, Leiotriletes sp., Lycospora pusilia, mal structures. The age of the litho stratigraphic unit s is Mic roreticulatisporites con cavus and Proprisporites still poorl y constrained. Only shales of the PQG, laevigatus. Reworked Visean and Toumai sian palyno recovered from a road cut north of Azinheira de Barros morphs were also determined. The SN Biozone, a local village provided a moderately preserved miospore zone, was defined by the presence of abundant assemblage that contains Verrucosisporites nitidus, the Anaplanispo rites baccatus, Densosporites intermedius , index species and the following taxa Crassispora sp., D. brevispinosus, Lycospora pusilla , Knoxisporites trira Densosporites spitsbergensis, Geminospo ra lemurata, G. diatus, K. stephaneph orus; Raistrickia nigra , Savitrispo spo ngiata, Punctatisporites sp., Retispora lepidophyta, rites nux and rare RotasporaFacta, Diatomozonotriletes Rugospora radiata and Vallatispo rites sp. that indicate sp. and Triquitrites marginatus. The NC Biozone is the LN Biozone. The VSC show s two main volcanic 62 Z. PE REIRA, J. M ATOS, P. F ERNANDES & J. T. OLIVEIRA suite s: one dominated by felsic volcanics, shales and 3.3 . T he Baixo Alentej o Flysc h Group intrusive diabases; the other composed mostly of basic volcanics and intrusives. The VSC suite is followed by The Baixo Alentejo Flysch Group (BAFG) comprises the Mertola Fm. turbidites that yielded a moderatel y mostly gravity flow sediments that form a continuous and preserved miospore association Crass ispora sp., southward prograding unit (Figure I). Sedimentological Densosporites spp., Lycospora pusilla, Microreticula and palaeontological data ofthe GFBA indicate it consists tisporites concavus, Proprisporites sp. and Wa ltzispora of three format ions, the Mertola, Mira, and Brejeira planiangulata, in association to the nominal species Formations (OLIVEIRA et al., 1979; OLIVEIRA, 1983; OLIVEIRA Raistrickia nigra. This assemblage is assigned to the NL &WAGNER-GENTIS 1983). The stratigraphic palynology local Biozone of mid late Visean . of the Baixo Alen tejo Flysch Group, although still very Palynostratigraphic research in the Ce re al anticline incomplete, has been provisionally established . The (westernmost Iberian Pyrite Belt) is currently being studied. miospore ages are consi stent with ammonoid data recov The lithostratigraphic sequence is still poorly constrained ered from all the BAFG units (KORN, 1997). in terms of lithology and age, and only very recent and limited data is available. The inves tigated Elf Aquitaine Mertola For mation boreholes, located in the antiform central sector, SW of Salgadinho, revealed the VSC Cereal felsic volcanics, a The Mertola Fm . was studied for palynomorphs in large sequence (>250m) of dark grey shales, with siltit ic several regions: such as the Neves Corvo mine , Mertola interc alations and minor quartzwakes and quartzites. town, Azenhas section in Guadiana River, Bens Farm, These shales yielded very well preserved specimens of and are give a late Visean age (OLIVEIRA et al., 2007 ; Grandispora echinata together with Ancyrospora spp., PER EIRA et a!., 2007). Three miospores biozones of late Apiculiretusispora sp., Auroraspora macra, Cristicava Visean age are identified: the NL and SN Biozones, tispora dispersa, Diducites poljessicus, D. mucronatus, defined as local Miospore Biozones (see the details D. versabilis, Emphanisporites annulatus, Grandispora described in the SWSP below) based respectively on the cornuta, Punctatisporites spp., Retispora macroreticu first occurrence of the index species Raistrickia nigra lata, Retusotriletes phillipsii, R. planus, R. triangulatus, and Savitrisporites nux, and the NC Biozone (recognized R. rugulatus, Rugospora explicata and R. radiata. This only at the Neves Corvo mine region) based on the first assemblage indicates the VH Biozone of late Famennian appearance of the key speci es Bellispores nitidus. age. All samples studied contain rich assemblages of acritarchs and prasinophytes. This assemblage is similar to those described for the Neves Corvo and Mina de Sao Mira Formation Domingos mines (Pere ira 2006a,b inc. ref.). No Carbon i The age ofMira Fm. is late Visean to early Bashkirian, ferous palynomorph assemblage s have been identified based on the ammonoids Dombarites, Lyrogoniatites and until now. This data confirm the antiform Cereal struc ture and will be compared with the upper sequences of Cravenoceras (OLIVEIRA et al., 1979; KORN, 1997). Palynostratigraphic data are scarce at the present time and the VSC , located in the eastern and western antiform are only restricted to black shale samples obtained in the sectors. Castro Marim region. These sample s yielded late Visean In the Spanish region ofGerena, in the eastern part of NC miospore Biozone assemblages that contai n the key the Val Verde del Camino Anticline, the PQG was dated early Frasnian base on a moderate preserved assemblage species Bellispores nitidus. of mio spores that includes Chelinospora concinna, Cristatisporites triangulatus , Geminospora lemurata , Brejeira For mation Retusotriletes rugu latus, Aneurospora greggsii and Verrucosisporites scurrus (LAKE, 1991; GONZALEZ et al., The youngest unit of the BFGA is the Brejeira Fm. 2D04; GONZALEZ, 2005). These assemb lages are ana lo The palyno stratigraphic study of this unit revealed 6 gous to those recovered in the Pulo do Lobo Antiform miospore biozones, ranging from the Bashkirian to late (Ribeira de Lima s and Gafo Fms .) and also the reworked Moscovian (PEREIRA 1997; 1999; Figure 5, 6). The se assemblage recovered in the upper part ofthe PQG in the miospore ages are consistent with the local ammonoid Neves Corvo mine region. biozonation (KORN, 1997). r§. § l:l.. ~ (j.. Caneiros Beach Road Cut Alfambras-lagos, Road Cut Alfambras-lagos, River cut Aljezur g ~ Km 164,9 (Pincho) Km ISS,S (Bensafrim) '"cs Ci I 'g I ~ OT(T.pseudo thiesseni ij I 2 I ~ I SS(C5aturml , Jg..., . 01 (T.ps(;'udothiessenlfl I {3 ,I ~ / , cQ, / , s.. , / , '"~ ? I or (7: pse udothiessenil) / ,E SS(C satuml S- NJ (F),t,iorl J ~ / I ~ ~ Sl (T.secwe. R. aculeata( / , 0; , / / , ~ , '/ , t;: ~ , ~ F ~.", O1i9ue7~ 1 & st(T. se 55 !C. satufntl S f FRIR.reticufatus) Blackshales and siltites EIH.' :f. _____ ~Lr==r 1~6~i ~ Studied sampleand -1- Miospore Biozones Sl {r securisl I Fig. 5 - Selected stratigraphic section from Brejeira Fm. (Adapt. PEREIRA, 1999). 0\ w 64 Z. PEREIRA, J. MATOS, P. FERNANDES & J. T. OLIVE IRA The base of the Brejeira Frn., in the north part of its marked by the occurrence of Thymospora psedothies outcrop area indicates the FR miospore Biozone of the senii, and the common presence of T obscura and T mid Bashkirian age, which contains the index specie thiessenii. This distribution of the palynological assem Reticulatisporites reticulatus and the Dyctiotriletes blages, confirms the southwestward progradation of the probireticulatus in the upper part of the zone. Further turbidites. The Variscan tectonic deformation in this south, miospore assemblages are successively assigned sector is Kasimovian in age. to the following: SS Biozone characterized by the index specie Cirratriradites saturni; Ra Biozone assemblage containing Radiizonates aligerens; Ra/NJ biozonal 3.4. Southwest Portugal Sector (SPS) boundary was only identified in Pincho Road section and (Bordeira and Aljezur Anticlines) is marked by the first occurrence ofFlorinites junior; the SL Biozone was identified based on the first appearance The stratigraphic succession of this sector was given of Torispora securis, the presence of Cadiospora in OLIVEIRA et al. (1985), OLIVEI RA et al. (1986), RIBEIRO magna and upper in the series by the incoming of the et al. (1987), PER EIRA (1997, 1999) and KORN (1997). index taxa Raistrickia aculeata; the OT Biozone is Four successive formations were identified in SPS, from A N ATLANTIC OCEAN LEGEND SedimentaryCovet BaixoAlentejo Flysch Group D BrejeiraFormation Carrapateira Group • Quebradas Formation MU!TalfB:OFormation BordaleteFormation r:::::I Iercenas Formation ''____....-:-2OCOm Fig. 6 - Geological Map ofAljezur and Bordeira Anti forms in SWPS (Adapt. SILVA et al., 1990). Devonian and Carboniferous palynost ratigraphy ofthe South Portuguese Zone, Portugal - An overview 65 base to top. the Tercenas, Bordalete, Murracao and presence of Cyrtospora cristifera, Puctatisporites irra Quebrada s Formations, of which the latter three are sus, Retusotriletes incohatus, Secarisporites sp. and combined to form the Carrapateira Group (Figure 6). Tumulispora malevkensis. The base of HD biozone, Detailed palynostratigraphic research has allowed the marked by the first incoming of the index taxa establishment of 12 miospore biozones, with 47 late Crista tisporites hibernicus, identified in the Eirinhas Devonian and more than 200 Carboniferous miospore Rizada-Penedo Road section , is also characterized by the species documented (PEREIRA et al., 1994; PEREIRA et al., first appearance of the distinctive species Umbona-tis 1995; PEREIRA, 1997; 1999). These palynostratigraphic porites distinctus and Neoraistrickia cymosa. A typical, results correlate well with the local ammonoids biozona diverse and very well preserved PC miospore Biozone tion (KORN, 1997). assemblage was recovered from several sections of the Bordalete Fm. The zone is defined by the presence ofthe guide specie Spelaeotriletes pretiosus together with Tercenas Formation Auroraspora macra, K. cf. triradiatus, Granulatisporites microgranifer, Neoraistrickia cymosa, N. logani, Rais The Tercenas Fm. (base unknown) comprises dark trickia clavata, Spelaeotriletes balteatus, Vallatisporites marine shales with interbedded thin sandy tempestites microspinosus, V vallatus, V verrucosus, Verrucosis which grades upward to a 10m thick tidal sandstone porites congestus, V irregularis and V nitidus (Figure 7). body. Rare clymenids, brachiopods and corals suggest a At the top of this unit the CM miospore Biozone of late late Famennian to early Toumaisian age for this unit Toumaisian age is missing, probably due to the presence (OLIVEIRA, 1990). The palynological study reveals a of a hiatus. These palynostratigraphic data exclude the diverse well preserved miospore assemblages assignable existence of a basal hiatus as previously suggested to the LN miospore Biozone of late Strunian age and VI (OLIVEIRA et al., 1985). miospore Biozone ofearly Toumaisian age (Figure 7). The LN Biozone is characterized by the common presence of Densosporites spitsbergensis, Dictyotriletes fimbriatus, Murracao Formation Knoxisporites concentricus, Retusotriletes crassus, Retispora lepidophyta, Rugospora radiata, Va llatispo The Murracao Fm. is composed oftwo members. The rites pusillites, Vallatisporites verrucosus, Tumulispora lower Pedra das Safias Member, has a thickness of 25 rarituberculata and the key specie Verrucosisporites metres and is composed of grey shales with rhythm ic nitidus. All samples suited contain rich assemblages of marly carbonate and dolomitic intercalations. The acritarchs and prasinophytes. member has yielded a few fragmentary macrofossils of corals and trilobites, including large but poorly preserved specimens of Merocanites sp., indicating an early to Bordalete Formation middle Visean age. The upper Vale Figueira Member has a thickness of 32 metres and is best exposed at the Atlantic The Bordalete Fm. is a monotonous succession of coast, near Carrapateira village. Strongly weathered dark grey to black shales and siltstones, which successions of the formation also occur in the area of frequently contain phosphatic nodules. Goniatites are Aljezur and Bordeira. However in the Quebradas beach randomly distributed within the Bordalete Frn., and section, the Vale Figueira Member is well exposed and in being concentrated at certain horizons and where they non-weathered conditions. Here, it is composed of belong to only one species, Becanites algarbiensis dark-grey or black shales, and nodular and sometimes (PRUVO ST 1914; KORN, 1998). In terms of palynos dolomitic limestones. The sucession contains scarce tratigraphy, the Bordalete Fm . allowed the identifica benthic faunas, restricted to certain levels characterized tion of the VI, HD and PC Miospore Biozones of by rare trilobites, brachiopods, echinoderms and rugose Toumaisian age (Figure 7). The VI miospore Biozone corals , The section is also extremely rich in goniatites (recognized in the Eirinhas-Rizada-Penedo Road and bivalves such as Posidonia becheri BRONN, 1828, of section, Monte do Penedo and Pedra Ruiva sections) is late Visean age. The following goniatite zones were iden marked by th e presence of the index specie tified (KORN, 1997): hudsoni Zone (fauna with Goniatites Vallatisporites verr ucosus together with the common hudsoni), crenistia Zone (fauna with Beyrichoceras sp.), 0\ 0\ Quebrad as Beach Road Bordei ra-Carrapateira Corte da Velha Marianos Road Eirinhas-Rizada-Penedo Pedra Ruiva 300 ~:i i .... . f PC {5. prl'tlosusl ! 21 or- ::; m ;;;,. Devonian and Carboniferous palynostratigraphy of the South Portuguese Zone, Portugal - An overview 67 sp irifer Zone (fauna with Goniaitites spinifer and The basal part of the NC Biozone is marked by the Goniatites fimbr iatusi, gracilis Zone (fauna with Hiber presence ofthe guide species Bellispores nitidus, which nicoceras carraunense) and postriatum Zone (fauna with was recognized in the Quebradas Beach section. The Lusitanoceras algarviense). The Murracao Fm. has been assemblage also contains the species Crassispora interpreted as a deep open-marine, pelagic carbonate maculosa, Microreticulatus concavus, Propisporites platform in front (to the south) of the flysch basin laevigatus, Raistrickia nigra and S. nux. (OLIVEIRA et aI., 1985; HERBI G et al., 1999). The palynostratigraphical evidence indicates that the The palynostratigraphic study of the Murracao Fm. entire Visean may be represented in the Murracao Fm. has recognized 5 miospore biozones of Visean age (PEREIRA 1997, 1999). (PEREIRA, 1999; Figure 2, 7). The study of the Pedra das Safias Member proved to be very difficult due to the strong dolomitization. Only in the Aljezur Anticline, in Quebradas Formation the Marianos and Corte da Ve1ha sections (Figure 7), where the unit has a more shaly character, it has been The Quebradas Fm. has a thickness ofapproximately possible to identify the base ofthe Pu miospore Biozone, 70 metres and is mainly composed of black shales with based in the first appearance ofLycospora pusilla and the intercalated carbonate and phosphoritic layers, lenses base of TS Biozone, by the first appearance of and nodule s (Figure 7). This unit is rich in fossils, and Knoxisporites triradiatus and K. stephanephorus. These several carbonatic horizons 'contain distincti ve ammo two miospore biozones indicate an early Visean age for noid assemblages (OLIVEIRA et aI., 1985; KORN , 1997). ' the Pedra das Safias Member. In a lower horizon, an indistinctive Cravenoceratoides The Vale Figueira Member, in Praia das Quebradas (?) sp. sugge sts an Arnsbergian age. High er up, some of section (Figure 7) has yielded moderately preserved the goniatite zones between the Ria to 02 are represented miospore assemblages assigable to the NL, SN, and NC by characteristic goniatites, including Vallites kullmanni Biozones of late Visean age. Two zones were defined as KORN, 1997, Reticuloceras reticulatum (PHILLIPS<, 1836), local miospore Biozones, the NL (Raistrickia nigra - Pro Reticuloceras coreticulatum BISAT & HUDSON, 1943, prisporites laevigatus) and SN (Savitrisporites nux) Bilinguites gracilis (BISAT, 1924), Bilinguites metabilin based respectively, on the first occurrence of Raistrickia guis (WRI GHT, 1927) Cancelloceras cf. crencellatum nigra and Savitrisporites nux guide taxa (Figure 2). (BISAT, 1924), Gastrioceras listeri (SOWERBY , 1812) and These biozones were defined due to the absence of Gastrioceras angustum (PATTEISKY, 1964). stratigraphically useful taxa such as Rotaspora spp. , The moderately preserved miospore assemblages Tripartites spp . and Triquitrites spp. Nevertheless, the recovered from Quebradas Fm. are assigned to the NL biozone can be correlated with the Raistrickia nigra Bashkirian KV and FR miospore Biozones. The KV - Triquitrites marginatus Miospore Biozone of Western Biozone is marked by the presence of Crassispora Europe based in the first appearance ofRaistrikia nigra kosankei. The basal pat of the FR Biozone is defined on that occurs at the same level. Proprisporites laevigatus the first occurrence of Reticulatisporites reticulatus appears together with the first R. nigra in southwest together with common specimens ofCrassispora kosankei, Portugal, but in Western Europe the first record of this Raistrickia fulva and S. nux (Figure 2). These results fit specie is much higher, at the top ofNC Biozone oflate well, in terms of age, with the local ammonoid biozona Visean to early Serpukhovian (CLAYTON et al., 1977, tion (KORN, 1997). CLAYTON, 1996). The SN local biozone can be corre lated with the VF miospore Biozone ofWestern Europe, based in the first occurrence of Savitrisporites nux. In CONCLUSIONS Western Europe, in addition to S. nux, the Tripartites . vetustus Biozone is defined by the first appearance of a Devonian and Carboniferous palynomorphs are group of new species which includes Tripartites vetus documented from all the geological domains recognized tus, Tripartites nonguerikei, Rotaspora fracta and R. in the SPZ . For the first time, an assessment ofall ofthe knoxi, which are not represented in the late Visean of palynostratigraphic record s obtained in the SPZ are southwest Portugal (CLAYTON et aI., 1977; CLAYTON compared (Figure 2). Twenty three miospore biozones 1996). are identifi ed in the SPZ comprising the identification of 68 Z. P EREIRA, J. M ATOS, P. F ERNA NDES & J. T. O LI VEIRA more than ISO Devonian miospores and acritarchs speci es (7) First appearance of Savitrisporites nux. Thi s and more than 200 Carboniferous miospore species local event is equivalent to the Western Europe fir st (PEREIRA et al., 2007). Selection of the index species used appearance of Tripartites vetustus Sche mel. In the for the SPZ is based upon the con sistent occurrence of SPZ, the othe r taxa th at typically oc cur with the S. nux each taxon in several sections and boreholes. are Rotaspora spp. and Grandisp ora spi nosa of lat e A number of palynological events recognized in the Visean age; Western Euro pe were identifi ed in the SPZ. These events, (8) Extinction of the characteristic Visea n miospore generally defined as the app earance or disapp earance ofa single genus or whole complexes of forms, providing species, Raistrickia nigra, Grandispora spinosa, Rotas important indicators in the establishme nt of global zona pora spp. and Crassispora maculosa, analogous to the tion s (CLAYTO N, 1985 ; CLAYTON, 1996; CLAYTON et al., Visean/Serpukovian bondary of the Western Europe ; 2003; OWENS, 1996 ; OWENS at aI., 2004; STREEL, 1996). (9) Appearance of the distinctive Bashkirian genus One eve nt has local importance at the scale of SPZ (in Reinschospora and increase on Crassispo ra kosankei, Portugal and Spain) and two events are locally distin ct representative ofthe early Bashkirian assemblages, similar and are correlated with goniatit es control points in the to the Western Europe; BAGF and SPS (see figures 2 and 7). The most important events identified in the Western (10) First appearance of Radiizonates aligerens, a Europe and recognized in SPZ are: type event for the late Westphalian A, in Western Europe. (1) Th e first app earance of Grandispora cornuta, It is also characterized by the increase of Laevigatos together with other taxa that typi cally occ ur at this level porites and Cirratriradites satu rni; in .SPZ, that incl udes Retusotriletes phillip sii, Diducites (11) First appea rance of Torispora genus, marking the versabilis and Rugospora radiata. This event, with the basal Westphalian C, as documented for Western Europe; same type assemb lage is recognized in Western Europe and marks the basal part of the VCo Biozone of late (12) First appearance of Thymospora spp. which in Famennian age (MAZIANE et aI., 1999); Western Europe marks the basal part ofthe Westphalian D. (2) First appearance of Grandispora echinata. Ass emblages in the SPZ also typically con tain consis The synopsis of the SPZ palynostratigraphy obtained tently Ancyrospora sp. , Cristicavatispora dispersa, from all the geological domain s recogni zed allow the Rugospora explicata and Teichertospora iberica at this followin g conclusions (Figure 2): level. It is worth noting that this assemblage is currently only documented in the SPZ and could represent a local 1. Early Frasnian miospores assemblages we re event. In addition, the appeara nce of Grandispora echi recovered from the PQG of the IPB, in Valverde nata occurs immediately before the first inception of del Camino Anticline, SW Spain (LAKE, 199 I ; Retispora lepidophyta in SPZ and Western Europe, at the GONZALEZ et al., 2004; GONZALEZ, 2005) and late Famennian age; app ear as reworked assemblages at the top of this (3) Extinction of Retispora lepidophyta. In Western sam e Group. The se Frasnian assemblages are also Eur ope th is ev ent is approx imately at the De vo comparable to those found in the Ribeira de Limas nian/Carboni ferous boundary (PAPROTH& STREEL, 1972; and Ga fo Fm s. of the Pul o do Lobo Antiform HIGGS & STREEL, 1984 ); (PEREIRA et al., 2006). (4) First appea rance of Spelaeotriletes pretiosus, 2. Late Fam ennian assemblag es in SPZ have a markin g the middle Tournai sian age, in Weste rn Europe; co nsistent presence of the m iospore sp ecies (5) First appearance of Lycospora pusilla. In Western Ancy rospora sp., Cris ticavatispora disp ersa, Europe it is approximately coincident with the Tournai Rugospora explicata and Teichertospora iberica. sian/Visean boundary; The se assemblages were recovered from the PQG (6) First appearance of Raistrickia nigra, together and the VSC (IPB ) (GONZALEZ et al., 2004 ; with other taxa that typi cally occur at this level in the PEREI RA et aI., 2004; 2007) and from the upper SPZ is Propisporites laevigatus and Densosporites spp.. units of the Pul o do Lobo Antifo rm (Horta da Thi s event marks the mid late Visean in SPZ. Thi s data is Torre, Santa Iria and Represa Fms ; PEREIRA et al., confirmed with goniatites; 2006a, b). Devonian and Carboniferous palynostratigraphy ofthe South Portuguese Zone . Portugal - An overview 69 3. Analogous late Strunian miospore assemblages (1996) - Mississippian Miospores. In: Palynology: Principles . were recovered from the IPB, the upper part ofthe and applications. JANSONIUS 1. & MCGREGOR D.C, (eds.), Am. Assoc. Strat. Palynol. Found, Vol. 2, pp. 589-596. PQG (CUNHA and OLIVEIRA, 1989; OLIVEIRA et al., CLAYTON, G., COQUEL, R., DOUBINGER, J., GUEINN K. J., LOBOZIAK, S., 2004; OLIVEIRA 2005; MATOS et al., et al., 2006), OWENS, B. & STREEL, M. (1977) - Carboniferous Miospores and the VSC in Spain (GONZALEZ, 2005) and also of Western Europe: illustration and zonation. Meded. Rijks from the Tercenas Frn. in Southwest Portugal Geo!. Dienst 29, pp. 1-71. (Bordeira and Aljezur Anticlines). CLAYTON, G., MCCLEAN,D. & OWENS , B. (2003) - Carboniferous pali nostratigraphy: recent developments in Europe (Abstract 4. Similarities in Upper Devonian miospore assem 103). International Congress on Carboniferous and Permian blages, strongly suggest that the Pulo do Lobo, the Stratigraphy , Utrecht, August 2003 . IPB basin and the Tercenas Fm . (Southwest CUNHA T. & OLIVEIRA 1. T. (1989) - Upper Devonian Palynomorphs Portugal), were part of the same palaeogeographic from the Represa and Phyllite- Quartzite Formation, M ina de Sao Domingos region, Southwest Portugal. Tectonos realm during the late Devonian. tratigraphic implications. Bull. Societe Beige Geol., 98 (3/4), pp. 295-309. 5. Records of Toumaisian palynomorphs from the EDEN, C. P. (1991) - Tectonostratigraphic analysis of the Northern Bordalete Fm, in Southwest Portugal and Extent ofthe Oceanic Exotic Terrane, Northwestern Huelva reworked Toumaisian associations in the VSC of Province. Spain. PhD thesis. Univ. Southampton, 281 pp. the IPB show the presence of the same taxa. FANTI NET, D., DRESSEN, R., DUSAR, M. & TERMIER, G. (1976) - Faunes famenniennes de certains horizons calcaires dans la formation 6. The VSC of the IPB yield miospores of late quatzitophylladique aux environs de Mertola (Portugal meri Famennian to mid/late Visean age (OLIVEIRA et al., dional). Comunicacoes Services Geologicos de Portugal, 60: 1986; OLIVEIRA et al., 2004; 2005; 2006; PEREIRA pp.121-l38. et al., 2006; 2007) . Mid/late Visean assemblages GIESE, v., REITZ, E. & WALT ER, R. (1988) - Contributions to the stratigraphy of the Pulo do Lobo succession in Southwest appear to be very consistent along the SPZ as the Spain. Comunica coes Servicos Geologicos de Portugal, 74, same assemblages are recorded from the BAFG. pp.79-84. GONzALEZ, E, MORENO, C., LOPEZ, M. J., DINO, R. & ANTONIOLI, L. (2004) - Palinoestratigrafia del Grupo PQ del Sector mas ACKNOWLEDGEMENTS oriental de la Faja Piritica Iberica, SO de Espana. Rev. Esp. Micropaleont., 36, 2, pp. 279-304. This work was presented at the CIMPLISBON'07 GONZAL EZ, E (2005) - Las pizarras negras del limite Devonico/carbo meeting and was sponsored by the project POCI/CTE nifero de la Faja Piritica Iberica (S.o. de Espana) . Estudio bioestratigrafico e implicaciones sobre la paleogeografia de -GIN/56450/2004 (pYBE) and POCI/CTE-GEX/60278/2004 la cuenca y el origen de las mineralizaciones de sulfuros. (PROVENANCE) of Fundacao para a Ciencia e Tecno Tesis Doctoral. Facultad de Ciencias Experimentales, logia, Portugal. Departamento de Geologia, Area de Estratigrafia, Universi The authors express sincere thanks to the referees, dad de Huelva, 200 pp . Prof. Ken Higgs (UNIVERSITY College Cork, Ireland) HIGGS, K., CLAYTON, G. & KEEGAN, B. J. (1988) - Stratigraphic and and Prof. Geoff Clayton (Trinity College, Dublin, systematic palynology of the Tournaisian rocks of Ireland. Geol. Surv. Ire!. Spec. Pap. 7, pp. 1-93. Ireland) that improved the manuscript. HIGGS, K. & STREEL, M. (1984) - Spore stratigraphy at the Devonian -Carboniferous boundary in the Northern "Rheinisches Schieferebirge" Germany. Cour.Forsch.Tnst. Senckenberg, REFERENCES 67: pp. 157-180. HIGGS, K.T., AVKHIMOVITCH V. 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( 1996) - Palynologic al (1994 ) - The Beja-Acebuches Oph iolite : Geolog ical caracter techniques-processing and mi croscopy. In: Palyn ology : ization and geodynami c significance. Boletim Geologico Principles and applications. JANSONIUSJ. & MCGREGOR D.C, Mineiro, 105, pp . 3-49. (eds.), Am . Assoc . Strat. Palynol. Found, Vol I, pp. 29-50. Artigo recebido em Dezembro de 2007 Aceite em Dezemb ro de 200 7 PLATES 74 Z. PEREIRA, J. MATOS, P. FERNANDES & J. T. OLIVEIRA PLATE I Plate captions list the taxonomic name of the figured specimen, followed by the formation, sample number, slide number and microscopic coordinates. Verrucosisporites bulliferus RICHARDSON & McGREGOr, 1986, Ribeira de Limas Formation, Sample 3-1, 1190-218. 2 - Cristatisporites triangulatus (Allen) MCGREGOR & CAMFIELD, 1982, Gafo Formation, Sample 13-2, 1315-165. 3 - Cristatisporites sp. cf. C. inusitatus (Allen) MCGREGOR & CAMFIELD, 1982, Ribeira de Limas Formation, Sample 3-3, 1260-228. 4 - Aneurospora greggsii (McGregor) STREEL INBECKER, BLESS, STR EEL & THOREZ, 1974, Gafo Formation, Sample 13-3, 1290-100. 5 - Chelinospora concinna ALLEN, 1965, Ribeira de Limas Formation, Sample I-I, 1320-205. 6 - Teichertospora iberica GONZALEZ, PLAYFORD & MORENO, 2005 , Horta da Torre Formation, Sample 7-2b-1450-185. 7 Grandispora echinata HACQUEBARD emend. UTTING, 1987, Horta da Torre Formation, Sample 8-2,1015-246. 8 Grandispora cornuta HIGGS, 1975; MP3 Borehole, Represa Formation, Sample 36,60-1 , 1305-225. 9 - Cristicavatispora dispersa GONzALEZ, PLAYFORD & MORENO, 2005 ; Open pit Mina de Sao Domingos mine, Represa Formation, Sample EM4-1 , 1225-185. 10 - Ancyrospora sp., Horta da Torre Formation, Sample 8-1,1440-120. II - Rugospora explicata GONZALEZ, PLAYFORD &MORENO, 2005, Horta da Torre Formation, Sample 7-3, 1505-200, INETI 0712. 12 - Rugosporajlexuosa (Jushko) STREEL, 1974, Horta da Torre Formation, Sample 7-la, 1390-105, INETI 0713. 13 - Retispora lepidophyta (Kedo) PLAYFORD, 1976; Tercenas Formation, Sample 105,1, 1350-210. 14 - Indotrirradites explanatus (Luber) KEDO, 1963; Tercenas Formation, Sample 106,b,2, 1391-165: 15 - Verrucosisporites nitidus (Naumova) PLAYFORD, 1964; Tercenas Formation, Sample 338,1,1110-110. Devonian and Carboniferous palyno stratigraphy of the South Portuguese Zone, Portugal >An overview PI. I 3 14 15 50 flm 76 Z. PEREI RA, J. MATOS, P. FER NANDES & 1. T. OLIVEI RA PLATE II Plate caption s list the ta xonomic name of the figured specimen, followed by the formation, sample number, slide number and microscopi c coo rdinates. - Cyrtosp ora cristifers (Luber) emend. VAN DER ZWAN, 1979; Bordalete Formation, Sample 147,c,3, 1155- 120. 2 - Cyrtosp ora cristifera (Luber) emend. VAN DERZWAN, 1979; Bordalete Formation, Sample 147,c,2, 1198-120, equatorial. 3 - Umbonatisporites distin ctus CLAYTON , 1971 ; Bordalete Formation , Sample 336, 3, 1245-1 48 . 4 - Granulatisporites microgranifer IBRA HIM, 1933; Bordalete Fo rmation, Sample 226 ,1, 1053-215. 5 - Tumulispora rarituberculata (Luber) PLAYFORD, 199 1; Bordalete Fo rmation, Sample 324,1, 1465- 138 6 - Spelaeo triletes balteatus (Playford) HIGGS, 1975; Bord alet e Formation, Sam ple 147,4, 1345-195 . 7 - Spelaeotriletes pretiosus (Playford) NEVES & BELT, 1970; Bord alete Form ation, Sample 247,4, 1354-65. 8 - Lycospora pusilla (Ibrahim) SCHOPF, WILSON & BENTALL, 1944; Murracao Formation , Sam ple 280,1,1220-175. 9 - Ly cosp ora p usilla (Ibrahim) SCHOPF, WILSON & BENTALL, 1944; MDS IBorehole, VSC , Sampl e 255, 30-1, 1155-75. 10- Densosporites sp.; MDS IBorehole, VSC, Sample 255, 30- 1, 1095-135. I I- Raistrickia nigra LOVE, 1960; Murracao Formation, Sampl e 379,1, 1455-73 . 12 - Knoxispo rites stephanephorus LOVE, 1960; Murracao Formation, Sample 379 .1 - 082-240. 13 - Knoxisporites triradiatus HOFFMEISTER, STAPLIN & MALLOYsensu SULLIVAN, 1964; Murracao Formation, Sample 147,2, 1145-120 . 14 - Rais trickia nigra LOVE, 1960; MD SI Borehole, VSC , Sample 359, 40- 1,1380- 180. Devonian and Carboniferous palynostratigraphy of the South Portuguese Zone, Portugal - An overview PI. II 1 2 4 6 8 9 11 13 78 Z. PEREI RA , J. MATOS, P. FERNANDES & J. T. OLIVEI RA PLATE III Plate ca ptions list the ta xonomi c name of the fig ured specimen, followed by the formation, sa mple number, slide number and mi cro scop ic coordina tes . - Savitrisporites nux (Butterworth & Williams) SMITH & BUTTERWORTH , 1967; Murracao Formation, Sample 387 ,2, 1160-255. 2 - Bellisp ores nitidus (Horst) SULLI VAN, 1964; Murracao Formation, Sam ple 229 .2 - 1368-210. 3 - Crassispora kosankei Potoni e & Krcmp eme nd BHARADWAJ, 1957; Quebradas Formation, Sample 387 ,2, 1230-95. 4 - Retic ulatisporites reticulatus (Ibrahim) [IJRAHIM , 1933; Quebradas Formation, Sample 195,1, 1364-35.. 5 - Raistri ckia fulva ARTUZ, 1957; Quebr adas Formation, Sample 200 ,1, 1430-205 . 6 - Cirratriradites saturni (Ibrahim) SCHOPF, WILSON & BENTALL, \944; Brejeira Format ion, Sample 266 ,1, \260-87. 7 Dictyotriletes probireticulatus (Ibrahim) BUTTERWORTH & MAHDI, \981; Breje ira Formation, Sample 238 ,b, l , 1350-110. 8 - Radiizonates aligerens (Knox) STAPLIN & JANSONIUS, 1964 ; Brejeira Formation, Samp le 242,5,1240-210. 9 - Florinites junior POTON]E & KREMP, 1954; Breje ira Formation , Sample 229,3, 1145-100. 10 - Torispora securis BALME, 1952; Breje ira Forma tion, Sample 63,1, 1135- 185. 1\ - Raistrickia aculeata KOSANKE, 1950; Brejeira Formation, Sample 63.1 - 1385-200. 12 - Cadiospora magna KOSANKE, 1950; Brejeira Formation, Sample 62, \ ,\ 254- 175. 13 - Thymospora pseudothiessenii (Ko sanke) WILSON & VENKATACH ALA, 1963; Brejeira Formation, Sample 63,1, 1220-185 . 14 - Thymospora obscura (Kosanke) WILSON & VENKATACHALA, 1963; Brejeira Formation, Sample 63,4,1045-65. Devonian and Carboniferous palynostratigraphy of the South Portuguese Zone. Portugal - An overview PI. III 1 2 3 4 7 8 10 11 50 ~ m 13 14