I Rivista ltaliana di Paleontologia e Stratigrafia r-olume numero

PALYNOSTRATIGRAPHY OF THE MUFARA FORMATION(MIDDLE.UPPER TRIASSIC, SICILY)

NICOLETTA BURATTI'I E ALEXIS CARRILLAT'!"

Receioed December I 5, 2aAA; accepted JanwatT 29, 2AA2

Key-uords: Sicilv, Middle-Upper Triassic, Ladinìan, Carnìan,biostratigraphv, pa11'nomorphs, conodonts, Camerosporites secatns

Phase.

Riassunto. Nelle successioni del Triassico Superìore della Sicii-ia nord-occidentale sono state rjconosciute quJttro rs'ociazioni pali-nologiche. L'analisi palinologìca della Formazione X,fufara ha con-tribuito, insicme ai dati relativi a rarì conodonti, alla costruzione diuno schema biostratigrafico che va dal L:dinico superiore al Carnicosuperiore. Questo intervallo di tempo viene qui interpret.rto in termi-ni dr"Camerosporites secatws phase". Nell'ambito di questa fase sì è cer-cato di riconoscere una progressir-a diversificazione dei taxa addizion-ali, sulla base dell'evoluzìone composizionale delle associazioninconoscrute.

L'associazione A è caratterizzata dalla presenza di elementiquali For.teosporites risscheri, Gordonispora fossulata, Se//aspord rugo,úer

rucata, \Xleylandites magmus e Enzonalasporites oigens, caratteristici delpassaggio Ladinico-Carnico e dalla comparsa dei primi elcncnti crrni-ct, Patinasporites densus e Vallasporites ignacíi, tnsteme con Lln gruppo"long-ranging" di predominanti bisaccati. Questa associazione è inoltre.egn.rta dali a.'ent t di LLmerosporires secatus.

Nell'assocìazìon e B, C. secatus è presente in modo discontinuoed è associato ad alcune forme eià presenti nell'associazione preccdcnrc(P densus, V ignacii, E. .oigens, Praecirculina granzfer Patittsporitesnovimundanus). Ar.ttrisporites tenuìspinosus, Klrtontisporis erv-ii, Stría-toabìeites aytugii compaiono per la prìma vòlta e, insieme conFoteo sporite s ùss cheri, G ordonispora fo ss ulata e S ellaspora rugof,- errucaar. permcttono di riferire l'associazione al CordevoLco-Julico inferi-ore..

L'associazione C è caratterizzata dalla presenza dt C. secatus, Pdensus, E. vigens, V ignacìi, P granifer, Duplícisporites granulatus e da

forme che scompaiono nello Julico e nel Tuvalico inferiore (rispettiva-mente Partitisporites nocímundanus e Lagene/la martinii). Questa com-posizìone può considerarsi di transizione tra quella dell'associazioneprecedente (8, Carnico inferiore) e la successiva (D, Tuvalìco).

Sulla base deila persistenza di forme presenti nelle :ssoci.:rz-ioni

precedenti, quali C. secatus, P densus, E. t,igens, V ignaciì e sulla base

delle prime comparse di Partitisporites quadruplícis e Samaropctllenites

speciosus, I'associazìone D viene riferita al Tuvalico (Carnico superi-ore) .

Abstract. The study of 10 sections of the Mufara Formation innorthern Sicily yielded four palynomorph associations rangrng rn age

from late Ladinian/early Carnian to late Carnian, and identified a trend

in the compositionai evolution of the assemblages within theCamerosporites secatus phase. The primary goal of this study was tocreate a composite section of the Mufara Formatìon, giving a tentatrve

srratigr:phrc order to the l0 investigated successions on the basis ofpalynomorphs range intervals.

The oldest assemblage (A) is dominated by long-ranging bisac-cates but is characterìsed bl rhe prcsence of transirional Ladinian-Carnian taxa such as Fot,eosporites uisscheri, Gordonispora fossulata,Sellaspora rugouetrucdtd,'Weylandites mdgmus and Enzonalasporitesvigens, and by the incoming of the firrt Carnirn eìements, Patinas-porítes dertsus and Vallasporites ignacii. Assemblage A is distinguishedfrom the )'ounger ones (B-D) by the absence ol Camero:porites se(a-

Assemblage B includes taxa which are present also in assem-

blage A (P densus, V. ignacii, E, oigens, Praecirculina grani.fer and Par-tìtisporites no"-ìmundanus). Camerosporites secdtus, Aratrisporitestenuispinosus, Kytomisporis ercii and Striatoabieites aytugii occv lorthe first time and, with the last occurrences of E'oisscheri, G. Jòssulata and.l. rugof,-errucat.t, indìcate that this assemblage is of Cordevolian-early Juìian age.

Assemblage (C) comprises an associatìon of Camerosporitessecatus, Patínasporites densus, Enzona/asporites o-ígens, Vallasporites

ignacìi, Praecirculina granifer and Dupliciporites granulatus, and taxa

with LADs (Last Appearance D:rum) in rhe Julian and the earlyTuvalian (P nov-imundanus and Lagenella mdrtiniì respectìvclv). Thisassemblage may be interpretecl as transitional between assernblage Band D.

Assemblage D comprises a typical Carnian association o{C amerosporite s s e catus, Patinasporites densus, Enzonalasp orites o igens

and Vallasporites ignacii, and includes the first occurrences oî Partí-

tisporìtes quadruplicis and Samaropollenites speciosus, which indicate a

Tuvalian substage (late Carnian) age.

Introduction

Following the work of Martini er aL. (1991,a,b), an

attempt was made to improve the biostratigraphic char-acterisation of the Mufara Formation (Schmidt di Fried-berg et al. 1960). The palynological study of several suc-

cessions which lack significant faunal elements, exceptfor sparse conodonts, was carried out. Stratigraphic reia-tionships between the different successions are not eas-

'tUniversità degli Studi di Perugia, Dipartimento Scienze delìa TercaPtazza Università 1, 06100 Perugìa, Italia, e-maìl: stradott@unipg.rt'f'flJniversité de Genève, Dépt. Géologie et Paléontologie l3 Rue des Maraîchers, 1211Genève 4, Suisse, e-mail: carriliata@;'stavanger.oil-

field.slb.com

102 N. Buratti & A. Canillat

Fig. 1 - Geographic location of the ten sections investigated: 1)

Pizzo Montanello, 2) Torrente Cuba, 3) La Pizzuta, 4)Cozzo Paparina, 5) Gambanera, 6) Cerda-Nicosia, Z)

Cozzo Tabaranì, 8) Monte Mufara, 9) Valle Faguara, lO)Vicari.

ily resolvable in the field because of the complexity ofthe tectonic setring and srrucrural framework. The paly-nomorph stratigraphic potential was used to provide a

useful biostratigraphic framework, an essential basis forfurther investigations.

The study showed also a trend in the composi-tional evolution of the palynological assemblages and a

progressive diversification within the Camerosporitessecatus phase (Visscher & Krystyn 1978).

Historical background

The study area exrends from the Madonie Moun-tains in centrai norrhern Sicily, west of the Palermoregion, to the north of the Sicani Mountains in north-west Sicily (Fig. t). These mountains comprise a seg-ment of the Apennine-Maghrebid chain, which is thedominant structural element in northern Sicily and isformed by mainly east/wesr-trending nappes in a foldand thrust belt. The nappes incorporate carbonate, sili-cÒ-carbonate and siliciclastic sediments, and result fromthe deformation of pre-existing paleogeographicdomains, platforms and pelagic basins formed during theMesozoic regional extension phase (Catalano & D'Ar-genio 1978; 1,982; Catalano et al. 1928).

In the Early Miocene, the collision of the Sardin-ian Block with the African margin initiated the forwardmigration of the thrust belt-foredeep sysrem and thedeformation of the paleogeographic domains frominternal to exrernai zones (Catalano et al. 1978; Cata-lano Ec D'Argenio 1978;1982; Broquet et al. 1984).

Originally the Mufara Formation was described as

comprising varicoloured, blue, green, purple, reddish,grey or black clays or marls wirh thin intercalations ofdolomitic limestone. The formation was named after thelocality in the eastern Madonie Mountains where it wasfirst measured and studied (Schmidt di Friedberg et al.1960) . However, its lower boundary was not observed at

thls slte.

Caflysch (1966) identified some Halobia sp.,

Daonella sp. and rare Tractrtyceras sp. in the Mufara For-mation, and considered this assemblage to be Late Tri-assic.

In addition to Halobia sp., Mascle (1967)observed some foraminifera (Rectoglandwlina cf. simp-soensis Tappan, Dentalina cf. cassiana Gúmbel, "Cornws-pira" liasinaTerq, Lenticwlina cf. cassiana Gùmbel) andostracods (Simeonella sp.), indicative of a Late Triassic

Subsequently, Senowbari-Daryan & Abate (1986)observed Carnian reefal elements, Ladinian (Anisian?)dasycladacean grainstones, and Norian Cayewxia bind-stone and pisoid facies in lenses of reworked materialintercalated in the marly levels of the Mufara Formation.

Martini et aI. (1991a. b) investigated outcrops ofthe Mufara Formation at localities in the Palermo andMadonie mountains and reported miospore assemblagescontaining Camerosporites secatus, Duplicisporites granu -latus, Praecirculina gantfer Patinasporites densws andSamaropollenites speciosus from marly intervals. Themiospores indicated a late Carnian age, which was con-firmed by conodonts extracred from calcarenites (Mar-tini et al. 1991,a,b).

More recenrly, Di Stefano et al. (1998) describeddeposits corresponding to the Mufara Formation fromthe Monte Altesinella (central Sicily). Those depositscomprise deepwater marls and limestones, containingradiolarians, halobids and conodonts, and interbeddedgravity-flow calcarenites and calcirudites. Di Stefano etal. (1998) attributed the association with Gladigondolel-la tetlrydis and Paragondolella polygnathifurmis to a mid-Carnian (Julian) age.

Location of the sections

The sections are located along a norrh\ilesr-sourh-east belt from the Palermo Mountains ro the MadonieMountains, encompassing the provinces of Palermo,Enna and Caltanissetta (Fig.2,3). The exact position ofthe productive secrions is described below, from wesr roeast:

Pizzo Montanello section (Palermo Mountains,Panormide Domain; latitude: 38o06'30"N, longitude:13"09'51"E) (Figs. 1, 2). The section crops out on a roadwhich connects Carini to Montelepre along rhe easrernflank of PizzoMontanello 064 m). The 50 m thick suc-cession is characterised mainly by marls intercalatedwith limestones. calcarenites and rare calcirudites.

Torrente Cuba section (Palermo Mountains,Panormide Domain; latitude: 38o05'32"N, longitude:1.3"1.3'82"8 ) (Figs. l, 2). k is located in the VailoneVaddi Cuba (between Montelepre and Monreale) andconsists essentially of intercalations of marls, marlylimestones and calcarenites (15-20 m).

La Pizzuta section (Palermo Mounrains, Imerese

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Palynostratigraphy of the Mufara Formation 105

Domain; latitude: 38'00'40"N, longitude: 13'1.5'1.7"8)

(Figs. 1, 2). It is located north of LaPizzuta (1333 m)and is accessibie from a road east of Portella de11a Paglia.The succession is 15 m thick and is formed, at the base,

by marly limestones, followed by maris and, in the upperpart, by limestones.

Cozzo Paparina section (Palermo Mountains,Imerese Domain; latitude: 38'01'62"N, longitude:13"16'43"E) (Figs. 1,2). The secrion crops out near theroad from Portella della Paglia to Altofonte; it is charac-terised by a 2A m thick intercalation of yellow marls,silty marls and marly limestones.

Vicari section (Palermo Mounrains, TrapaneseDomain; latitude: 37"49'51"N, longitude: 13"34'4I"8)(Figs. 1,2). The outcrop is located along the road to thevillage of Vicari (650 m) before the last curve. ft is char-acterised by a 10 m thick succession of dark marls, marlyIimestones and calcaren ites.

Cerda-Nicosia section (Termini Imerese, Cerda-Roccapalumba unit; latitude: 32"55'59"N, longitude:13'50'99"E) (Figs. 1, 3). The succession crops out alonga dirt a road located on the eastern side of highway A 19.

A 4 m thick outcrop shows a large block of bioclastic tobrecciated limestone embedded in silty marls.

Cozzo Tabarani section (\lestern Madonie Moun-tains, Cerda-Roccapalumba unit; latitude: 37o54'52"N,Iongitude: 13"51,'71"E) (Figs. 1, 3). The ourcrop is to theeast of highway A 19, along the river Imera and sourh ofCozzo Bonforti. The section (40 m thick) is dominatedby limestone levels, followed by silty marls and calcare-ous siltstone intervals.

Monte Mufara section (Madonie Mountains,Panormide Domain; latitude: 3Z'51'80"N, longitude:14"0A'71"8) (Figs. 1, 3). The secrion crops our on rhewestern flank of Monte Mufara (1865 m). It is a 40 mthick succession characterised by limestones and chertylimestones, intercalated, upwards, with marly intervals.Calcarenites and marly limestones also occur along thesection.

Valle Faguara section (Madonie Mounrains,Panormide Domain; latitude: 37o51'21"N, longitude:14'02'84"E) (Figs. 1, 3) . The succession is a few hundredmeters south of Rifugio Marini on rhe road to Petralia,between the first and second bridge. A 40 m thick sectioncrops out showing a base composed mainly by lime-stones.

Gambanera section (Caltanissetta Basin, Imerese-Sicano Domain; latitude: 37"29'A2"I\, longitude:14"46'47"8) (Figs. 1,3).It crops out in a small quarrir,5km south of Sferro, in the direction of Castel di Iudica.It consists of a 1,2 m thick succession of alternatingmarly clays and marls, with limestones and calcarenires,with increasing carbonates towards the top.

Methods

Standard preparation techniques were used

F;o 4 Distributìon of palvnomorphs in the Vicari section.

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Lithology

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Late Ladinian/early Carnian

age

o Krauselisporites sp

O \4inutosaccus sp.

a Densosporites sp.

O Klausipollenites sp.

o Retitriletes sp.

.l Schizosaccus sp

o Cycadopites sp

a Parillinites sp. I

a Sellaspora sp.

o P s eudo enz o na las p o r i les s ummus

a o Protodiploxypinus sp.

o Pityosporites sp.

a Lundtisporites dcufus

o o Triadispora sp.

o 3 o rdon isp or a fos sulata

o a Staurosaccítes quadrífdus

o o Par acir cul i na v errucos a

a Platysaccus papilionis

o S ellaspora rugoverrucata

O lup Ii cisp orites verrltcos us

o o lup I i c is p o r ítes granu la tus

a leltoidospora minor

o 'eylandites mdgmus

O 'or) e os p o r i tes v is s cher i

o a nz o n a la s p oril es v i gens

a o allasporites ignacii

o atindsporites densus

o lquisetosporites sp.

o lvalipo llis ps eudoalatus

a )alamospora sp

O 'raecirculina sraní{er

CERDA-NICOSIA SECTION

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106 N. Buratti & A. Carrillat

for miospore recovery (Faegri & Iversen 1975:'

Doher 1980; Heusser & Stock 1984; Vood et al.

1996) and for conodont extraction (Vrielynck 1987).

Upper Triassic chronostratigraphy: historical back-ground

Some current controversies regarding theammonoid-based subdivision of the Carnian stage mustbe introduced briefly before discussing the palynologicalrecord of the Mufara Formation.

The Carnian stage was introduced by Mojsisovics(1869) for the stratigraphic interval corresponding tothe Tracbyceras aonoides Zone. Laîer, Mojsisovics et al.

(1895) redefined the stage, and divided it into theCordevolian, Julian and Tuvalian substages, correspon-ding to the Tracbycera.s aon, Trachyceras aonoides, andTropites subbwllatus ammonoid zones, respectively.

Despite a common acceptance of this zonationscheme, objections were raised and alternatives wereproposed. For example, after a biostratigraphic study ofthe Hallstatt Limestones, Krystyn (1978) proposed thesubdivision of the Alpine-Mediterranean lower Carnianinto four ammonoid subzones which together form twozones that chàracterise a single substage. He consideredthe taxonomic difference between Trachyceras aon andT.aonoides to be insufficient to justify the use of these

species tnzonal subdivision. He also proposed to use Z

Fig. 6 - Distribution of palynomorphs

in the Pizzo Montanello sec-

tion.

aon for defining the basal sub-zone of the Julian substage(Krystyn 1,978). Hence theCordevolian substage wouldbecome superfluous and need tobe rejected.

As a consequence, ofKrystyn's (1978) concept, the

lower Carnian can be defined interms of two zones (Aonoidesand Austriacum) and four sub-zones (Aon, Aonoides, Austri-acum. and Sirenites). The pro-posed rejection of the Cordevo-lian substage was not accepted

by, ..g., Visscher & Brugman(1981), Van der Eem (1983),

Bìzzarrrnt et al. (1989) and Urlichs (1994). Regardingthe San Cassiano Formation, Van der Eem (1983) argued

that the ammonoid faunas wrth "Trachyceras aon mdyjustify Urlicbs (1974) proposal of establisbing d. type-sec-

tion for the Cordeaolian Substage in the type-area of the

formation". Mostly based on the ammonoid biostratigra-phy of the Southern AIps, and especially of the Prati diStuores section (Urlichs 1974), the original zonation ofMojsisovics was thought to be stili valìd, and conse-quently Urlichs (1994) retained the Cordevolian sub-s tage.

Investigations by Broglio Loriga et al. (1999) inthe Prati di Stuores/Stuores \Wiesen section suggest thatthe base of the Carnian Stage should be placed at theFAD (First Appearance Datum) of Daxatina cf.

canadensis. Other considerations support this proposal,among them the fact rhar the first appearance of the tra-ditional Carnian genus Tracbyceras with species differentfrom Trachyceras don occurs within the lower Daxatinacf. canadensls Subzone. Another consideration is thatthe section is located in the type-area of the Cordevoliansubstage of Mojsisovics et al. (1895) and of Urlichs

Q97a; 199a). This last argument may also emphasize theneed for redefining and maintaining the Cordevoliansubstage. In order to facilitate comparisons with previ-ous palynological studies in the Alps, the classic three-foid subdivision of the Carnian stage is accepted in the

Present Paper.

Palynostratigraphy

Interpretation of the Camerosporites secatus phase.

Any work on the palynological characterisation of theCarnian stage cannot avoid considering the"Camerosporites secatus phase" concept. This was intro-duced by Visscher & Krystyn (1978), on the basis ofSchuurman's (1977;1979) Phase I, in order to provide a

practical palynological tool for correlation. Theydescribed this characteristic assemblage as a phase dis-tributed in many paleofloral provinces, reflecting a late

Ladinian-Carnian interregional microflora development.The Camerosporites secatus phase (Visscher tr

Krystyn 1928; Cirilli 8. Montanari 1994; Cirilli tggS;Warrington 1996) includes a rapid diversification of theCircumpolles group, and is represented by Praecìrcwlina

Pafunostratigrapby of the Mufara Formation t07

Distribution of palynomorphs

in the Monte Mufara section.

granifer, Camerosporites secatus

and Duplicisporites granulatws rnassociation with the vesicatespecies Patinasporites densws,

Enzonalasporites aigens, Vallas-

porites ignacii and Psewdoenzon-

alasporites summus. The phase

was originally considered to be

an exclusively Carnian event,but later was extended into theLadinian (Visscher & Brugman1981; Vai der Eem 1983; Besems

1981a, b, 1983; Besems tr Simon1982; Dolby k Balme 1976;Brugman et al. 1994). Occur-rences are also known fromearly, middle and late Carnianassemblages from well-datedammonoid-bearing successions.

such as the Prati di Stuores sec-

tion in the Dolomites (BroglioLoriga et al. lllv) in ltaly, whereC. secatus has been recordedfrom the base of the Daxatinacf. canadensis Swbzone (lowerCarnian).

In Austria the occurrenceof C. secatus is well controlledby a continuous ammonoidzonation which covers the entire

Carnian stage (Dunay 8r Fisher 1978). These authorsrecorded the appearance of C, secatus in the Trachyceras

aon Zone (Cordevolian substage) and its persistenceupwards into the Halobia rwgosa/Carnites floridus Zone(Julian substage) and Tropites subbwllatws Zone (Tuvaliansubstage).

The presence of C. secatus in late Carnian assem-

blages was confirmed by palynostratigraphic data com-ing from a section in Sicily (Visscher & Krystyn, 1978),

where it was recovered from the Tropites subbwllatws

Zone or the "Anatropltes-Bereich", indicative of theTuvaiian 3 substage (uppermost Carnian). The wide dis-tribution of the C. secatus phase is demonstrated by itspresence in the Alpine Triassic of Europe (Visscher &Brugman 1981), Italy (Van der Eem 1983; Broglio Lori-

t08 N. Buratti & A, Carrillat

ga et al. 1999), southern Albania (Cirilli Er Montanari1994), Israel (Cirilli and Eshet 1991), Africa (Bour-mouche et aI. 1,996), the USA (Fisher & Dunay 1984;Litwin & Ash 1,993), Arctic Canada (Fisher Ec Bujak1925), Australia (Dolby & Baime 1926).

Because C. secatus ranges through the Carnianstage, it is unsuitable for a detailed biostratigraphic sub-division of that unit. Many authors (Dolby & Balme1926; Visscher & Brugman 1981; Van der Eem 1983;Besems 1981a, b; 1983; Besems & Simon 1982; Brugmaner al. 1994) tried to recognize composirional trendswithin the C. secatus phase and a subdivision at substagelevel was attempted, on the basis of a progressive diver-sification of associated miospore raxa.

The younger part of the phase is recognised by theincoming of taxa such as Paracirculina quadrupLicis andSamaropollenites speciosus in association with C. secatus(Visscher et al. t98O), hence the co-occurrences of C.secAtus, Vallasporites ignacii, Enzonalasporites cìgens andPatinasporites densus with P quadrwplicis and Samaropol-lenites specìoszs is considered indicative of the Tuvaliansubstage (Visscher & Krystyn 1928; Cirilli er al. D9A;Cirilli Sc Eshet 1991; Cirilli & Montanari 1994r Cirilli1995; Warrington 1996).

FiÙ R Distribution of palynomorphsin the Valle Faguara section.

Palynological assemblages fromthe Mufara Formation

In the present paper, s/e

attempted to recognize succes-sive qualitative steps in the com-positional development of paly-nological assemblages in theMufara Formation. Twenty onesections were investigated and 1O

proved productive (Fig. 2, 3)

yielding four distinctive andhighlv diversified palynologicalassemblages. The good preserva-tion of the organic material,together with the abundance anddiversity of the assemblages (Pl.1, 2) allowed useful stratigraphicinferences and a correlation,where possible, with conodontdata. The following assemblagesare recognised:

Assemblage A. The microflora is

characterised (Fies. 4, 5) by theoccurrences of Densosporites sp., Infernopollenites sul-catus, Weylandites magmus, Deltoidospora minor, Sellas-pora sp., Equisetosporires sp. and Psewdoenzonalas-porites summus which are exclusive forms of thisassemblage. A group of significant species, consistingof Gordonispora fossulata, Paracirculina oerrucosa, Sel-laspora rugoaerrucdta, Duplicisporites granulatus,Foveosporites oisscheri, Enzonalasporites vigens, Vallas-porites ignacii, Patinasporites densus, Praecirculinagranifer, and Partitisporites novimundanus occurs inassemblage A and, sporadically, in some or all the otherassemblages. These species are in association with a

considerable number of long-raneing sporomorphsdominated by bisaccates. The composition of thisassemblage is comparable with many orher Tethyanand extra-Tethyan assemblages. Patinasporites densus,Vallasporites ignacii and Enzonalasporites oigens areconsidered typical Carnian forms. Their presence wasreported from ammonoid-bearing successions in Aus-tria (Trachycertr.s Aon Zone; Dunay 8c Fisher 1978) andnorthern Italy (Regoledanws Zone and early part of theDaxatina cÍ. canadensis Subzone; Broglio Loriga et al.1,999;Yan der Eem 1983; Blendinger 1988). The associ-ation of these forms, rogether with the occurrences of

Dwplicisporites granulatui, suggests an affinity with theCamerosporites secatus phase. However Camerosporitessecatus is absent from assemblage A, and the vesicategroup (comprising P densws, E. vigens and V ìgnacii) isin association with Ladinian-Carnian boundary elementssuch as Foveosporites r,ìsscberi, Gordonispora fossulata,Partiti sp orite s noo im undan us, S ellasp ora rugoe errucdtaand \Xleylandites magmws. These Ladinian-Carnian formshave been recognised in Ladinian assemblages (Van derF,em 1983; Broglio Loriga er. aI. 1999; Blendinger 1988)and their LADs occur in the lower Cordevolian except

Palynostratígraphy of the Mufara Formation

Fìo 9

109

Distribution of palynomorphsin the Cozzo Tabarani section.

Fig. 10 - Distribution of palynomorphsin the Torrente Cuba section.

in the case of S. rugorterrucatawhich seems to reach the upperCordevoiian or loìMer Julian(Van der Eem 1983; Blendinger1 e88).

The main features thatallow the grouping of theseassociations in assemblage A are

the absence of Camerosporitessecatus in combination with theprese nce of a mixture of upperLadinian-Carnian and typicalCarnian elements. Thismicrolloral composirion mayreflect a transitional srage in thegradual change from a rypicalupper Ladinian association ro an

exclusively Carnian association.Assemblage A was found in theVicari and the Cerda-Nicosiasections (Figs. 4, 5). These sec-tions are therefore dated as lateLadinian-early Carnian. In theVicari succession, a conodontassociation characterised byGlad.igond.olella tethydis (P1. 3,

Fig. 3a, 3b) and Pseudozarkodi-na saginata was found (sampleCSI 218). This associarionranges from the lllyrian (upper

Anisian t to rhe upper Julian(Vrielynck 1982), rvhich is notin conflict with the palynologi-cal data.

Assemblage B. The microfiorais characterised by sporadic occurrences o{Camerosporites secatus in association with many specieswhich persist from the preceding assemblage A. Amongthese Gordonispora fosswLata, Foveosporites aisscheri andSellaspora rugox)errucdta disappear in this assemblage.Striatoabieites aytugii, Aratrisporìtes tenuispinosus, A.paenwlatus, and I{yrtomisporis eroii occur for the firsttime in association with many additional elements(Figs.6,7,8).

The composition of the assemblage B has a clear

110 N. Buratti G A. Carrillat

PLATE 1 - Spores and bisaccate pollen of the Mufara Formation

Pl. I

Fig. 1

Fìo 4

Fio 6

Frg.7FiO R

Fio c

.Weylandítes magmus, slide CSI222 oxa, (England Finerl: E

25-4, x9aa

Paracirculina quadruplìcis, CSI31 oxa, E-43, x500

Ijtrtomisporis ercii, CSIL4J oxa, O 26-2, x7O0

Duplicisporites granulatus, CSIlZ oxa, O-39, x1000

ProtodipLoxypinus americws, CSI206 oxa, J 29-1,x70AProtodiploxypinus fastidiosus, CSI3l oxa, E 25-1, x6OO

Lunatisporites acwtus, CSI222 oxa, H 29-2/4, x70A

OvalipoLlis psewdoalatus, CSI195 oxa, E 28-4, x500

Platysaccws papilionis, CSI222, E 28, x3O0

Fig. 10 P papilionis, CSI121 oxa, F 34, x500

Fig. 11 Falcisporites ot,ìfurmis, CSI56 oxa, G 28-3, x5OO

Fig. 12 Oulipollis pseudoaÌatus, CSI195 oxa, F 30, x600

Fig. 13 Cuneatisporites cerinus, CSI31 oxa, F 41-4, x6O0

Fig. 14 Staurosaccites quadri.fidus, CSI17 oxa, R 30-3, xSOO

Fig. 15 Voltziaceaesporites heteromorpba, CSI185 oxa, F 28-4, x500

Fig. 1 6 Vitreisporites pallidus, CSI1.9 oxa, N 39-4, x1 000

Ftg.17 Striatoabieites aytug'ii, CSI1.24 oxe, G l8-4, x6OO

Fìg. 18 Chordasporites cbinleanus, CSI56 oxa, B 39-3, x60O

Fig. 19 Klausipollenites sp., CSI31 oxa, J 43-2, x90O

PT,2 Palynostrattgraphy of the Mufara Formation

PLATE 2 - Spores and pollen of the Mufara Formation

111

Fig. 1 Paracirculina eerrucosa, CSI222 oxa, F 22-1, x8OO

Fíg.2 P. verrucosa, CSI222 oxa,H 29-4, xSAO

Fig. 3 Reticulatisporites dolomiticus, CSI19Z oxa, e 24-1, x8OO

Fig. a Aratrisporites tenuispinosus, CSI12l oxa, T Z1-4,x7OOFig. 5 Enzonalasporites ztigens, CSI19 oxa, S 32-1, x90OFig. 6 Foveosporites v-isscberi, CSI222 oxa,J 19, x5OO

Ftg.7 Pseudoenzonalasporites summus,CSIZZ2 oxa, H 3O-2, x60OFig. 8 Duplicisporites granulatus, C51246 oxa, S 2Z-4, x8OO

Fig. 9 Partitisporites novimundanus, CSI124 oxa, J 42, xSOO

Fig. 10 Deltoidospora minor, CSI222 oxa, E 3Z-3, xSOO

Fig. 11 Krauseltsporites sp.,CSI222 oxa,H22-1,x5OOFig. 12 Camerosporites secatus, CSI185 oxa, O 46-3, xTOA

Fig. 13 C. secatws, CSI25 oxa, F 23,x7OA

Fig. 14 Vallasporites ignacii, CSI22 oxa, G 4Z-4, x6aOFig. 15 Enzonalasporites oigens, CSI19 oxa, I 37-2,x7AOFig. 16 Vallasporites ignacii, CSI22 oxa, R 19-3, x6OO

Frg. 17 Patìnasporites densus,CSI22 oxa, M43, x5OO

Fig. 1 8 Gordonispora fossulata, CSI|21. oxa, J 40, x1 OOO

Fig. 19 Praecirculina granfer, C5126 oxa, M 30-211, xIOOO

Fig. 20 Lagenella martinii, CSI246 oxa, F 4O-4, xgOO

All the slides are housed in the Département de Geologie et Paléon-tologie, Univ. de Genève.

tt ttt ltt ttt tlil|ttlì|ilil|tltt ttt ttt trr rltttttltt ttltttttltt ttltttl!tiltttttttl)LJ):tt

Lithology-

NN

-ìc.hÉo.l

z

t\)(rì { @\o samples

Tuvalian só"

a oa a Verrucosisporites sp.

a.-l

a ? a O a-l Klausipollenites sp.

Plalysaccus sp.

olo'---ol;l iir

aio

ao

ao

----.f-ol

Aratrisporites sP.

En zona laspo r ites v igen s

Camerosp o riîes s eca tus

Ov a I ip o I I ís ps eudoa I a tus

a a C hordaspori tes chin leanus

o Parillinites sp

a Concavisporites sp.

o Dup licis p o r i t es verrucosus

o a o Dup I ic is p o r ites gra n u la tus

o a Vallasporites ignacii

--la o

oO a Patinasoorites densus

o ' ar a cir cu I ína q uadrup I i cis

a a o O 4lisporites sp.

a Vinutosaccus sp.

o )onverrucosisporites sp.

o l-unatis oorites acutus

.l 9taurosa cci tes quadrifdus

.l F a I c is p o r i tes ov ifo r m is

a, Luna t is p or i les noviau I ens ís

a P r a ecir cu I i na gr an ife ro piculatisporites sp.

a .1. Cuneatisporiles sp. ,

o Schizosaccus sp. r

oa

O

[-lt??!:::!' p

"p iri9Ii1 _

gellasporafot,eorugulata T

o Pityosporites sp.

a O Triadispora sp.

a lalamospora sp.

a Cycadopites sp

a Protodiploxypinus sp.

o Ovalípollis sp

112 N. Buratti ù A. Carrillat

Fig. 11 - Distribution of pall'nornorphs in the La Pizzuta scction.

resemblance with Carnian associations (Visscher trKrystyn 1978; Cirilli 1995), on the basis of the presence

of circumsulcate (Camerosporites secrrtus) and vesicateforms (Vallasp orite s ignaci i, Prae circ ulina gran ifer, Pati -nasporites densus). Some other elements allow a moredetailed age assessment. Apparent LADs of Gordonispo-ra fosswlata, Foaeosporites aisscheri and Sellaspora rugo.o-

errucata and the presence o[ I{yrtomisporis eraii (Van derEem 1983) confines the age to the early Carnian. Com-parison with Van der Eem's (1983) palynological study

of Carnian sediments in northern Italy suggests toattribute this assemblage to rhe aigens-densus phase(Corder.'olian, lower Carnian). The sporomorph compo-sition of assemblage B is recognised in the Pizzo Mon-tanello, Monte Mufara, and Vallone Faguara section(Figs. 6, Z, 8) dating them as Cordevolian-earlyJulian.

A conodont assemblage from the Monte Mufarasection (sample CSI 105) is composed of specimens ofGondolella sp. and Didymodella ahernata which suggest

a pre-Tuvalian age (Vrielynck 1987).

Assemblage C. The microflora is characterised bythe more or less continuous presence of Camerosporitessecatus, together with a significant group of taxa alreadypresent in assemblages A and B. The first incoming ofAratrisporites fischeri, Lagenella martinii, Angwstisulacitessp. and Camerosporites pseudoverruc.ttus was recorded,with the appcarance of A. fisheri and L. martinii beingthe most remarkable event (Fig. 9). L. martinii is knov'nfrom an ammonoid controlled succession in Austria,where it was recorded in the upper part of the Halobiarugosa/Carnites floridus Zone (Dunay & Fisher 1928),and elsewhere in Europe from the basal Cordevolian tothe Julian (Van der Eem 1983) and from middle Corde-volian to lower Tuvalian (Visscher & Brugman 1981).

On the basis of its biostratigraphic range, assemblage Cmay be interpreted as transitional between the precedinglower Carnian assemblage B and the succeeding upperCarnian (Tuvalian) assemblage D. Another significantdatum is the presence of Partitisporites noz,imundanusu'hich was not noted in assemblage D. The LAD of Pnoaimwndanzzs is in the Julian Substage densws-maljawk-inae phase (Van der Eem 1983).

The assemblage was recognised in the CozzoTabarani section (Fig. 9). The essentially transitionalnature is interpreted in terms of a mid-Carnian(Julian)/early Tuvalian age.

No conodonts were found in association with thisassemblage.

Assemblage D. The assemblage is characterised bya group of new microfloral elements, including Paracir-culina qwadruplicis, Samaropollenites speciosus, Voltzi-aceaesporites beteromotpha, Protodiplox?pinus americu s,

Reticulatisporites dolomiticus, Sellaspora fooeorugulata,Samaropollenites concinnus, Chordasporites cbinleanws,Aratrisporites sp., Falcisporites oatformis, Lunatisporitesnoaiaulensis, Triadispora vilis, T. aurea, Lycopodiaciditessp., Circella splendida, Pyramidosporites traz,erseì andMicrocachrydites fastidioides. Many of the additional ele-

ments recorded.in assemblages A, B and C are still pres-ent (Figs. 10, 1 1, 12, 13). Camerosporìtes secatus is abun-dant in all the sections bu Patinasporites densus occursonlv sporadically. The combined presence of Enzonalas-p orit e s v igen s, Val la sp orit e s igna ci i, D up I i ci sp o rit e s gran u -latus and Praecircwlina granifer, already characterising

Pa 11, n ostratì grap fu of the,\I ufara Fctrmation

Fie. 12 - Distribution oî pah.nomorphs ìn rhc Cozzo Pap:rrina Fig. l.isection.

assemblage C, the tte.a. elentents Paracirculina quadrupli-cls and Samaropollenites speciosus, must bc considered :rs

late Carnian (Ti:valian). A late C:irnian age appears ro beconfirmed bv the presence of some constituents of thesecondar\. group, Voltziaceaesporites heteromorpha, Pro-todiploxypinus (tmericus, Cbordasporites chinleanus, andLunatisporites notiaulensis, n'hich are ofren recordcd inUpper Carnian succe ssions from North America(Dunay 8r Fisher 1979; Fisher & Dunay 1984; Litwin etal. 1991), and b,v the absence of Partitisporites not-imun-danus.

The microfloral composition of this assemblage is

rccorded in many sections of the Mulara Forrnation,such as Torrente Cuba, La Przzuta, Cozzo Paparina and

113

Distribution of pah"norrorphs in the Ganbanera section

Gambanera (Fies. 10, 17, 12, 13) l'hich are rhereforereferred to the late Carnian (Tur.alian).

A conodont association recovered from the Gam-banera succession (samples CSI 23, CSi 30) is distin-guished by the presence of Paragondolella polygnatbi-

formis (Pl. 3, Fig. 2a, 2b) and Metapolygnatbus abneptis(Pì. 3, Fig. 1a, 1b); rhe occurrencc of these forms rs norin conflict rvith a late Carnian (Tuvalian) palvnologicalassemblage (Vrielynck 1987 . Di Stefano 1988).

Conclusions

This analysis enabled rhe construction of a paly-nostratigraphic framework for the Mufara Formarion,

+rl-rl-

+ t:+ta

{Lithology

o7H

zF

aF

oaaìz

! Nq

N oN! samples

Tuvalian age

a a a a 'u tteat isno ri tes . eri t nsa a :uneatisporites sp

a a a a a a friadispora sp

a a )valipollis ctrltus

a a a a a a a a a )vo I i pol I i s pseu d oul a I u s

a a a a )u o I i c i.s o o r it es s ra I u I úlus

a a a a a a o o Vallosporites ignacit

a a a a a a a iatnuropol len it es speci osus

a a a a a a a a a a a :anerosDoriles s ecalus

o a a o a a a ) 0rac i rcu li na quadrup I i c is

a a O a a a ol0ilto.tporo sp

a a Triadisporo vilís

a a a a a a a I n:o n a I as po r i te s v ige n s

a a a a a a a a )atiua.spoutes densus

a a a a 't I o tn Ò,t Do ra nrc\a:o iL n

a a 'i t re is po r i t es pal I ítl u s

a a a a a a ) | o I vs accus po pil t ott i s

a a a a a a ltisporites sp

a a ' raec i rt u I i na sra il i lè ta nsuslisulciles sD

a a onyerrucostsDornes sD

a a a a 'lausipollenites sp.

a Vitttttosaccus sp

a a ) ro totl tplol ypt u us sp

O a /erntcosisporites sp.

a 'o ltziacea es po rites sp.

a > tt ru c: i rc u I i nu ve rruc os a

o ) \' rat n i s n I f o ri I c s I ta re r.r e !

a D ro I otl t p ! o.rl p t n u s | | r t I i d i o \ u.\

114 N. Buratti & A. Carrillat

PLATE 3

Fìg. 1a Metapo\,gnathus abneptìs, juvenile form (220X, lateral vicn-)

Fig. 1b Metapolygnathus abneptis,juvenile form (220X, aboral vìew)

Fig.2a Paragondolellapolygnathìfurmis (150X,lateralvien-)Fig. 2b Paragondolella pol,gnathzformis (150X, aboral vien')

Fig. 3a Glddigondolelld tethydts lsAX,lateral vieu.)

Fig. lb Cladiy"nl"lcllt ierÀ;11 1150X. abonl rìe*7

and provided information on the deposition of the unitfrom the late Longobardianlearly Cordevolian (Ladin-ian-Carnian boundary) to the late Tuvalian (late Carn-ian). It represents an important base for successive inves-tigations, helping to understand the deveiopment of theMufara basin and its palaeoenvironmental evolution.Further investigations are needed to assess the exact

stratigraphic relationships between successions contain-ing assemblage A (Cerda-Nicosia and Vicari sections),assemblage B (Valle Faguara, Monte Mufara and PizzoMontanello sections) and D (Torrente Cuba, CozzoPaparina, LaPtzz,ura and Gambanera). The constructlonof a composite section of the Mufara Fm. was ettemptedon the basis of palynological data and the scheme depict-ed in Fig. 2 and 3 was drawn to explain the gradual diver-

sification of the associations; however, the hypothesis ofpossible lateral interfingering cannot be excluded.

Furthermore, the palynological analysis identifieda trend in the compositional evolution of the assem-

blages within the Camerosporites secdtus phase. Thistrend is characterised by the successive incoming of newtaxa within the C. secatus phase, which define four dif-ferent palynological assemblages.

This new evidence refines the strarigraphic frame-work for the Mufara Formation providing further per-spectives and causing repercussions to the attempts ofapplying the C. secatus phase in previous palynostrati-graphic studies (Dolby Er Balme 1976; Visscher & Brug-man 1981; Van der Eem 1983; Besems 1981a, b, 1983;

Besems & Simon 1982; Brugman et al. 1994).

Pl. l

Palynostratigrapby of the Mufara Formation 115

Acknoraledgements. The authors are grateful to G. \Warrington

and H. Visscher for their accurate and constructive reviews and to M.Gaetani for precious suggestions. The authors wish also to thankSimonetta Cirilli for fruitful discussions and improvements of themanuscript, and Louisette Zamnetti for making valuable suggestions.This work is part of a Ph.D. study, financially supported by the Swiss

National Science Foundarion (L. Zamnetri Grants 2O-50527.97, "LePermien et le Trias réthysien: étude et évolution des microfaunes etdes sédiments") and by "Progetto Ateneo, Cirpro 199912a00" (S. Cir-illi funds).

Species list

A listing of spores and pollen species identified and quoted in rhe text and

illustrated in the figures is given below:AlisporiteS rolzstzs Nilsson, 1 958

AratrisporitesJischerl (Klaus 1960) Playford & Dettmann, 1965

Aratrisporites paenuktws (I{lats 1960) Playford & Dettmann, 1965

Aratrisporítes tenuispinosus Plal'ford, 1965 (Pl. 2,Fig. a)

Cakmospora mesozoica Couper, 1958

Camerosporites secatus Leschik,1956 (P1. 2,Figs. 12, 13)

Camerospoites pseudovenucatus Scheuring 1 920

Chordnspontes cbinleanws (Datgheny) Dunay Ee Fisher, L979 (Pl. 1, Fig. 18)

Circelk splendida Sukh Dev 1959

Cuneatísporites cerinws Dol6y & Balme, 1976 (PL 1, Fig. 13)

Deltoid.ospora minor (Cotpe41953) Pocock, 1970 (P1.2, Fig. 10)

Duplicisporìtes granuktus Leschtk,1956 (Pl. 1, Fig. 4; Pl. 2, Fig. 8)

Duplicisporites Derrtrcosus (Leschik, 1956) emend. Scheuring, 19lO

Enzonaksporites zlgezs Leschik, 1956, (P1.2, Figs. 5, 15)

Falcnp orites ooiformis Dunay Er Fisher, 1979 (Pl. 1, Fig. 1 1 )

Fooeospoites oisscberiYanErve, l.9TT (Pl. 2, Fig. 6)

Gordonisporafossuku (Balme 797A)Yan der Eem, 1983 (Pl. 2, Fig. 18)

Infmopollenites sulcatus (Pattsch 1958) Scheuring, 1970

I(ynomzspons eruiiYan der Eem, 1983 (Pl. 1, Fig. 3)

Lagenella mattinii (Leschik, 1 956) ICaus, 1960 (Pl. 2, Fig. 2A)

Lunatisporites acwrzs Leschik, 1956 (Pl. 1, Fig. Z)

Lunatìsporites nooiaulensis Leschik 1956

Protodiploq,pinus fastidiosus (Jansonius) rWarrington 1974 (P1.1, Fig. 6)

Ooalipollìs cultus Scheuing, l97aCnalrpolhs pseutÌoaktzs (Ihiergan 1949) Schuurman,1976 eL 1, Figs. 8, 12)

Praecirculina granifer Leschlk, 1956 Klaus, 1960 (Pl. 2, Fig. 1 9)

Paracaculira quadrupàos (Scheuring 1970) Yan der Eem, 1983 (Pl. 1, Frg. 2)

Panitísporites notimundanus (Leschik, 1956) (Pl.2, Fig. 11)

Paracirculina Derrucosa Praehauser-Enzenberg, l97A @1. 2, Figs. 1, 2)

Patinasporites densus Leschlk,1956 (Pl. 2,Fig. 1.7)

Pk4,saccus papilionis Potonié Er K1aus, 1954 (Pl. 1, Figs. 9, 1O)

Protodiploxypinus americus Dunay Er Fisher, 1929 (Pl. 1, Fig. 5)

Pseudoenzonaksporites summus Scheuring 197A eL. 2, Fig. l)Pyramidosporites trarersei Dunay & Fisher, 1 929

Reticulatisporites dolomiticws Blendinger 1988 (Pl. 2, Fig.3)Samaropollenites speciosus Goubin, 1965 (P1. i, Fig. 19)

Samaropolbnites concinnus Fisher Es Dunay 1.974

Sellaspora rugopet'rucata Van der Eem, 1983

Staurosaccites quad.ifdus Dolby, in Dolby Er Balme,1976 (Pl. 1, Fig. 1a)

Strtatoabieites ayragl Visscher, 1966 (Pl. 1, Fig. 1/)Tiiad.ispora aurea Scheuring, 1970 emend. Scheuring 1978

Tiiadispora vilis Scheuring, 1970

Valksporites ignaciiLeschrk,lg56 (Pl. 2, Figs. 14, 16)

Voltziaceaespoites lseteromorpba Klaus, 1964 (Pl. t, Fig. 15)

Vitreisporìtes pallilzs (Reìssinger) Nilsson, 1958 (P1. 1, Fig. 16).We/andites

magmus (Bose Ee Kar 1966) Van der Eem, 1983 (Pl. 1, Fig. 1)

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