Upper Permian Radiolarians from the Sosio Valley Area ... · KOZURfound intheTorrente San Calogero...

Jb. Geol. B.-A. ISSN 0016-7800 Band 136 S.99-123 Wien, Juli 1993

Upper Permian Radiolariansfrom the Sosio Valley Area, Western Sicily (Italy)

and from the Uppermost lamar Limestone of West Texas

By HEINZ KOZUR*)

With 4 Text-Figures, 1 Table and 3 Plates

ItalienSizilien

USATexas

RadiolariaSystematik

StratigraphiePaleogeographie

Contents

Zusammenfassung 99Abstract. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 99

1. Introduction 1002. Geological Setting 1003. Systematic Part 1044. Paleoecologic Evaluation ofthe Radiolarian Faunas 1125. Biostratigraphic Evaluation ofthe Radiolarian Faunas 1126. Paleogeographic Implications 115

Acknowledgements 115References . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 122

Oberpermische Radiolarienaus dem Sosiotal (West-Sizilien, Italien)

und aus dem obersten Lamar-Kalk (West-Texas, USA)Zusammenfassung

Eine der reichsten oberpermischen Radiolarienfaunen der Welt wurde in roten Tiefwassertonen im Sosiotal (West-Sizilien) nachgewiesen. 4 neueGattungen und 4 neue Arten werden aus dieser Fauna beschrieben. Conodonten aus einer Kalkarenit-Einlagerung nahe der reichsten Radiolarien-füh-renden Probe erlauben eine Zuordnung zur Dzhulfa-Stufe. Die biostratigraphische und paläogeographische Bedeutung dieser Radiolarienfaunen wirddiskutiert.

Für Vergleiche mit der oberpermischen Radiolarienfauna von Sizilien wurde die Radiolarienfauna des obersten Lamar-Kalksteins von West-Texasneu untersucht. Im Gegensatz zu früheren Altersbestimmungen gehört diese Fauna nicht zur oberen Capitan-Stufe, sondern zur Dzhulfa-Stufe.Fol/icucul/us bispinosus n.sp. wird aus dieser Fauna beschrieben.

AbstractRed deep-water clays from the Sosio Valley area in Western Sicily contain one of the richest Upper Permian radiolarian faunas of the world. 4 new

genera and 4 new species are described from this fauna. Conodonts from a calcarenite intercalation near to the richest radiolarian-bearing sampleindicate a Dzhulfian age. The stratigraphic and paleogeographic importance of this deep-water radiolarian fauna is discussed.

For comparison with the Sicilian Upper Permian radiolarian fauna, the radiolarian fauna of the uppermost Lamar Limestone of West Texas wasre-investigated. In contrast to the previous age determinations this fauna is not of Late Capitanian, but of Dzhulfian age. Fol/icucul/us bispinosus n.sp.has been described from this fauna.

*) Author's address: Dr. sc. HEINZ KaWR, Institut für Geologie und Paläontologie, Universität Innsbruck, A-6020 Innsbruck.

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©Geol. Bundesanstalt, Wien; download unter www.geologie.ac.at

1. Introduction

Permian radiolarians have been so far described aboveall from the Circum-Pacific area (Japan, South China, Phi-lippines, Alaska, Western North America, Chile), from theCis-Urals, and from Texas.

KOZUR & KRAHL (1987) discovered the first Permian ra-diolarians from the Western Tethys (Crete, Greece) and DEWEVER, BOURDILLON-DE GRISSAC & BECHENNEC (1988)figured Permian radiolarians from Oman.

During a one-day excursion (autumn 1986) in the SosioValley area under guidance of Dr. P. 01 STEFANO,Palermo,KOZURfound in the Torrente San Calogero section near thefamous Pietra di Salomone limestone block for the firsttime pelagic South Tethyan Ladinian rocks with Daone//a,conodonts and radiolarians, and Lower Permian deep-wa-ter radiolarians (see CATALANO,01 STEFANO& KOZUR, 1988a, b, c).The discovery of Early Permian radiolarians in Western

Sicily drastically changed the former paleogeographicpicture of the Permian Tethys as shallow-water gulf in thearea of the South European Western Tethys.

The Circum-Pacific radiolarian fauna is dominated byAlbaillellacea. In the Lower Permian Cis-Uralian radio-larian faunas, in contrast, Albaillellacea are only a subordi-nate group. Radiolarian faunas of restricted basins or ofshallow-water environments both in the Circum-Pacificrealm and in the Cis-Urals are characterized by Copicyn-trinae KOZUR& MOSTLER.

In the Upper Permian of Japan, the oceanic Circum-Pa-cific radiolarian faunas can be subdivided in an openoceanic assemblage (mostly cherts) with Neoa/bail/e//aTAKEMURA & NAKASEKO and a marginal oceanic assem-blage (mostly claystones and siltstones) with the Fo//icucu/-Ius ? charveti group and without Neoa/bai//e//a. Some Albail-lellacea, like /shigaconus scho/asticus (ORMISTON& BABCOCK),occur in both assemblages.

However, it cannot be excluded, that these assem-blages have also somewhat different ages. In the Philip-pines, the Neoa/baille//a ornithoformis Zone follows above fau-nas with F? charvetiwithin a continuous chert sequence.

The Upper Permian radiolarian faunas of Western Sicilybelong to the marginal oceanic assemblage of the Circum-Pacific province. However, the Changxingian part of thered claystones has not yielded well preserved radiolarianfaunas.

For comparison, the radiolarian fauna of the uppermostLamar Limestone in the Delaware Basin, West Texas, havebeen investigated.

From these beds ORMISTON& BABCOCK(1979) have beendescribed the first Permian Albaillellacea. This radiolarianfauna (Fo//icucu//us ventricosus-/shigaconus scho/asticus fauna)was assigned to the Capitanian (Middle Permian) by OR-MISTON& BABCOCK(1979) and NAZAROV& ORMISTON(1985).This has caused difficulties by the age determination ofthe Japanese and Sicilian Upper Permian radiolarian fau-nas.

The discovery of Tethyan Dzhulfian conodonts in the up-permost Lamar Formation and in the post-Lamar/pre-Castile beds near the Guadalupe Mountains as well as inthe uppermost Altuda Formation of the Glass Mountains(KOZUR, in press), has solved the contradictions betweenthe ranges of the F ventricosus-1. scho/asticus fauna in Texas(Capitanian) and in Eurasia (Dzhulfian).

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2. Geological Setting

All here described Upper Permian radiolarians havebeen derived from the Torrente San Calogero section SWof the famous locality Pietra di Salomone in the Sosio Val-ley area SW of Palazzo Adriano (see Text-Fig. 1).The Permian and Triassic sequence of the Torrente San

Calogero section is part of the Sicanian paleogeographicrealm of Western Sicily described by CATALANO,01 STEFA-NO& KOZUR(1991,1992). The Permian and Triassic litholo-gic successions of the Sosio Valley area and the Rocca-palumbra-Lercara area are shown in Text-Fig. 2.The exposed sequence in the Torrente San Calogero

section (Text-Fig. 3) was described by CATALANO,01 STEFA-NO& KOZUR (1992). It begins with an Olistostrome Unit ofRoadian age (= basal part of Middle Permian GuadalupianSeries). These beds have been placed into the Kubergan-dinian by CATALANO, 01 STEFANO& KOZUR (1991, 1992).However, the Kubergandinian cannot be directly recog-nized in pelagic Tethyan beds without ammonoids.The Kubergandinian age was therefore concluded by

the position above Chihsian and below Wordian pelagicfaunas. Because the Kubergandinian is defined by fusuli-nid faunas that are restricted to central and eastern Te-thyan shallow-water deposits and missing in the wholewestern hemisphere and Boreal realm as well as in pelagicdeposits of the Tethyan realm, this Stage is unsuitable asinternational standard. Moreover, the stratotype lies sev-eral1000 m high in a hardly accessible area in the CentralAsian Pamirs and the rocks are thermally altered (CAI =4-5).Therefore the Kubergandinian has been replaced by the

now well-defined Roadian with an easily accessible stra-totype in the Glass Mountains, West Texas. It is well defin-ed around the margins of the Delaware Basin, where alsothe stratotype is situated. The most complete outcropsare on the opposite slope of the Delaware Basin, at thewestern slope of the Guadalupe Mountains, where boththe underlying Leonardian s.str. and the overlying Wordianare present in several continuous sections with pelagicand shallow-water fossils (ammonoids, conodonts, fusu-linids, radiolarians etc.).The matrix of the Olistostrome Unit contain few pyritized

radiolarians, identical with those described by CORNELL&SIMPSON (1985) and NAZAROV& ORMISTON(1985) from theupper Cutoff Formation that was in the investigated out-crop along the US Highway 62-180 SE of the GuadalupeMts. erroneously placed into the Bone Spring Formation.NAZAROV& ORMISTON (1985) placed the post-ArtinskianBone Springs Formation with Mesogondo/e//a idahoensis(YOUNGQUIST,HAWLEY& MILLER) and the overlying CutoffFormation with M. nankingensis (CHING) (= "Gondo/e//a" serrataCLARK & ETHINGTON)into the Artinskian, but this age de-termination was rejected by KOZUR& MOSTLER(1989). TheArtinskian-Kungurian boundary can be well correlated byconodonts with the middle Skinner Ranch Formation,where Neostreptognathodus pnevi KOZUR & MOVSHOVICHbe-gins. A little later Mesogondo/ella intermedia (IGO), Neostrepto-gnathodus fo/iatus (IGO), N. exscu/ptus (IGO) and in the upper-most Skinner Ranch Formation N. prayi BEHNKENand N. ida-hoensis YOUNGQUIST, HAWLEY & MILLER appeared. Theyoungest Artinskian yielded N. pequopensis BEHNKEN andMesogondo/e//a bisse/li (CLARK& BEHNKEN). It is at least 4 con-odont zones older than the upper Cutoff Formation, fromwhere the "Artinskian" radiolarians of the Bone SpringFormation at the US Highway 62-180 have been derived.


1)0 2)[]]]]] 3)1~ :14)~ 5)1'\'16)1 a,b...1 7)ITID8) ~ 9),. ""..... 10)A"'A' 11) S

1000

500

A'

c.S. Giorgio

.CALOGERO

N

to

In the light-gray limestones immediately below the pre-dominantly red claystones radiolarians are rather fre-quent, but badly preserved. Follicucullus porrectus RUDENKOand Ishigaconus scholasticus (ORMISTON & BABCOCK) havebeen determined. A Late Permian age can be assumed forthis radiolarian fauna.The richest radiolarian fauna occurs in the lower part of

the red claystones. The bad to well preserved fauna withmore than 100 000 radiolarians per kg sample weight is

.500mo

Text-Fig.1.Geologicmap (a) and cross section (b) ofthe TorrenteSanCalogeroarea,SosioVal-ley (WesternSicily, Italy). After CATALANO,01 STEFANO& KOZUR,1991.1 = Debris; 2-6 Upper tectonic unit: 2 =Cherty Limestones (upper Carnian-Rhae-tian); 3 = Grayplaty limestonesandmarls(Middle-lower part of UpperCarnian);4 =Gray and greenish, partly red cherts,greenishand pink nodular,often siliceous '.or cherty limestones, marls, in the lowerpart tuffitic intercalations (Anisian-LowerCarnian); 5 = Undifferentiated Olisto-stromeUnit,ClaystoneUnitandsiliciclast-ic deposits, limestoneconglomerates,redmicritic limestones (Permian: uppermostArtinskian-Changxingian, and LowerTriassic); 6 = Sosio Limestoneblocks (a =Rupedi SanCalogero;b = Pietradei Sara-cini; c = Rupedel Passodi Burgio;d = Piet-ra di Salomone).7 = Lower tectonic unit:Triassic-Miocenedeposits. 8 = Main tec-tonic boundaries.9 = Minor thrust planes.10= Crosssection line.S = Locationof the SanCalogerosection,from where the described radiolarians ofWesternSicily havebeendescribed.

The conodonts from the matrixof the olistostrome Unit give thesame age as the radiolarians.They yielded Mesogondolella phos-horiensis (YOUNGQUIST, HAWLEY &MILLER) and Sweetognathus subsym-metricus WANG, RITTER & CLARK.This is a typical Roadian cono-dont fauna. S. subsymmetricus is sofar only known from the Roadianof South China, but according to apersonal communication of Dr. L., LAMBERT,Iowa City, this species isalso present in the Roadian ofTexas.Siliceous micritic limestones

and dark, hard, limey marlsyielded very rich Lower Permianradiolarian faunas of latest Artin-skian to Early Leonardian age.Like all deep-water radiolarianfaunas, also this fauna consistsalmost exclusively of Albaillella-cea. This fauna has been de-scribed by KOZUR in CATALANO,01STEFANO & KOZUR (1989). In thispaper already some of the UpperPermian radiolarians, describedin the present paper, have beenfigured.The Olistostrome Unit is overlain by the Claystone Unit

that consists of gray, in the upper part predominantly red. deep-water soft claystones. The gray, yellowish weather-ing claystones from the lower part of the Claystone Unityielded a lot of Wordian conodonts with Mesogondolella sici-liensis (KOZUR), but only a few indeterminable radiolarianshave been found in these rocks. This part of the ClaystoneUnit is not exposed in the section SW of the Pietra di Sa-lomone.

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SYSTEM

T

srAGERhaetian

Norian

LITHOLOGY - FOSSILS

Pelagic gray bedded cherty calcilutites with intercalationsof calcarenites. Halobia, MonoUs, ammonoids, conodonts,radiolarians.

Text-Fig. 2.Restored stratigraphic schemeof the Permian and Triassic rocksof the Sicanian paleogeographicdomain of Western Sicily.Supplemented after CATALANO,01STEFANO& KOZUR(1991).

RUpper

Upper

Carnian Middle

Pelagic gray Cherty calcilutites with inter-calations of brown calcarenites and, at placescalcirudites, gray shales. Halobia, conodonts,radiolarians, ostracods, trace fossils.

Gray micriticsilic.limest.,

Pel. red clays, thiCkpartly sandy calcare-nites, calc. sandst.,conod., sponge spie.

Resedlmented calc-arenites, biogenic1s.Conodonts,sponge spicules.(OlistolithS)

wnite reef slope or oase-of-s loDe bio-genic limestones. Sponges, bryozoans,conodonts, holotnurian sclerites,ammonoids, crinoids.

Dark gray lime-stones. Brachiopodsammonoids, eChi-noderms, conodonts

scolecodonts,radiolarians,poromorphs. (Olistoliths)

Gray and redf lysen: gradedsandstones,partly fine-conglomeratic, siltstone, Shales.EC:'\inoderms, foraminifers,ostracods, conodonts, trace fossil dark-gray siltyCOlistoliths and sequences). " marls, marly Is.

Radlolarlans, conodonts.(Mostly olistolitns).

Olistostrome Unit: Gray softclaystone with reworked sand grains.Conodonts, ostracods, radiolarians,sporomorphs. Olistoliths from tne underlying rocks.

Gray, yello-wish weatheringred claystones.Conod., radiol.

Pelagic red deep-water claystoneswith few thin calcareniteS. Radio-larians, ostracods, foraminifers,conodonts, sponge spicules. Towardthe lower part increasingly light-gray intercalations.

Pelagic graded yellowish weatnering conglomeratic to calc-arenitic limestones with shallow-water clasts, grainsupported. Conodonts, foraminifers, i'\Olothurian sclerites.

Reddish pelagic:: calcilutites (Hallstatt Limestones), marls,yellowish weathering limestones, marls, limestone conglo-merates. Conodonts, foraminifers, ostracods, radiolarians

Pelagic greenish siliceous calcilutites with filaments,some tuffites. Conodonts.

Lower Pelagic greenisn-gray to pink nodular Cherty limestones,greeniSh-gray, rarely violet snales, subordinately thinred radiolarites. Daonella, "Posidonia" wengensis,ammonoids, conodonts (Gladigondolella, Pseudofurnishiusetc.) radiolarians, ostracods.Pelagic reddisn to greenish-gray nodular cnerty or siliceouslimestones, greeniSh tuffites, greenisn to gray radiolarites.Conodonts, radIolarians. Or: red siliceous limestones, cherts.

LeonardianS.str.

SUpper

Ladinian

S Middle Lower

Anisian (Upp,)

C Lower 01enek ian(Scyth.)

Brahmanian

p ChangxingianUpper

DzhulfianE

Capitanian

R WordianMiddle

RoadianM

LowerA

A

NArtinskian

Sakmarian Unknown

Asselian

102


o SOI(m=

SE NWText-Fig.3.Torrente San Calogero section. After CATALANO,DI STEFANO& KOZUR(1991, 1992).A = Olistostrome Unit (Roadian Stage, earliest Middle Permian age); B = Predominantly red claystones with few thin calcarenites, upper part of theClaystone Unit (Upper Permian: Dzhulfian-Changxingian); C = Bedded greenish and gray cherts, tuffites, siliceous and cherty limestones (LowerLadinian); D = Pink and greenish nodular, cherty limestones, marls, subordinately red cherts (Upper Ladinian-Lower Carnian) described in the presentpaper. It consists of a typical Upper Permian assemblage of Circum-Pacific character.

described in the present paper. It consists of a typical Up-per Permian assemblage of Circum-Pacific character.The accompanying conodont fauna is very poor and

consists of Clarkina sosioensis GULLO& KOZUR, C. changxingen-sis italicus KOZURand Hindeodus typicalis (SWEET).Clarkina sosio-ensis is a typical conodont for the Upper Permian deep-seaenvironment of the Sosio Valley area.It is also present in the Dzhulfian Neoalbaillella omithoformis

Zone (with N. omithoformis TAKEMURA & NAKASEKOand N.pseudogrypa SASHIDA & TONISHI) of the Kanto Mountains,central Japan (SASHIDA& TONISHI, 1985, PI. 7, Fig. 12, de-termined as Neogondolella sp.) and in Upper Permian chertswith Ishigaconus scholasticus of the Chichibu Belt of Japan(SUYARI, KUWANO& ISHIDA, 1983, PI. 1, Fig. 6, determinedas Gondolella cf. orientalis BARSKOV& KOROLEVA).A single, about 20 cm thick, broken calcarenite near to

the richest radiolarian faunas in the lower part of the redclaystones contains a very rich conodont fauna with theabove species.This conodont fauna was placed by GULLO & KOZUR

(1992) in the Upper Changxingian because of the pres-ence of Clarkina changxingensis WANG & WANG. However, therange of C. changxingensis in South China (Upper Chang-xingian including the transitional beds) is facies-control-led. This species invaded together with radiolarians theshallow-water sea during a slight deepening (or sea levelrise) in the Upper Changxingian. In fully pelagic deep-wa-ter deposits C. changxingensis begins already in the LowerDzhulfian, but the Dzhulfian representatives belong most-ly to C. changxingensis italica KOZUR. This subspecies domi-nates in the lower part of the red claystones, from wherethe richest and best preserved radiolarians have been de-rived.The upper part of the red claystones belong to the

Changxingian, indicated by C. subcarinata (SWEET)and otherChangxingian conodonts from thin, broken calcareniteswithin the red claystones. This part yielded unfortunately

only badly preserved radiolarians, mainly Phaenicosphaerasp. and Ishigaconus scholasticus (ORMISTON& BABCOCK).Except of typical Upper Permian and long-ranging

forms as well as new species of characteristic UpperPermian genera, very few forms of Capitanian (MiddlePermian) character are present. One specimen of Parafol-licucullus monacanthus (ISHIGA & IMOTO) was found amongseveral 100.000 specimens of Dzhulfian radiolarians.This species is a Capitanian guideform; reworking isprobable.An other typical Middle Permian species, Pseudoalbaillella

eurasiatica KOZUR, KRAHL& MOSTLERis present with severalspecimens. This species occurs also in Japan and on thePhilippines from the Middle Permian up to the Dzhulfian. Itis seemingly an autochthonous component of the Dzhul-fian radiolarian faljnas of Sicily, at least the forms withshort pseudoabdomen. The very rare specimens withlonger pseudoabdomen are probably reworked MiddlePermian specimens.The third Middle Permian element is Parafollicucullus con-

vexus (RUDENKO & PANASENKO). Only 4 specimens havebeen found. Reworking cannot be excluded, but also inOman this species is present in a Dzhulfian radiolarianfauna (see also systematic part).In West Texas, Upper Permian Albaillellacea are only

known from the uppermost Lamar Limestone Member ofthe Bell Canyon Formation. The Lamar Limestone cropsout in a long cuesta running across the western side of theDelaware Basin, SE of the Guadalupe Mountains in Cul-berson County, West Texas. The locality data have beenpublished in ORMISTON& BABCOCK(1979). The sections H,I, Nand 0 of this paper (for location see ORMISTON& BAB-COCK, 1979, Text-Figs. 1-2) have been re-sampled. In thepresent paper only a few radiolarians will be publishedfrom section H along the US Highway 62-180, about6.5 km SE of the Guadalupe Mountains, the type localityof Follicucullus ventricosus ORMISTON& BABCOCKand "F" scho-

103


Genus:

Subfamily:

Subclass:Order:Suborder:

lasticus ORMISTON& BABCOCK). Detailed papers about theradiolarians and other microfaunas of the Lamar Lime-stone are in preparation.

The holotypes of both Follieueullusventrieosus ORMISTON&BABCOCKand Ishigaeonus seholastieus (ORMISTON& BABCOCK)have been derived from the top of the Lamar Limestone inlocality H.ln these beds radiolarians are mostly moderate-ly frequent (about 50-100 specimens per kg sampleweight) and well preserved. These data are in agreementwith the data by ORMISTON & BABCOCK (1979). However,some samples from the uppermost 80 cm of the outcropyielded very rich assemblages with several thousands ra-diolarians per kg sample weight. These samples yieldedfor the first time Ishigaeonus seholastieus with fully preserveddorsal columella, very important for comparisons with Ishi-gaeonus fureus(CARIDROIT & DE WEVER)and the new Follieueul-Ius species F bispinosus n.sp.

The radiolarian fauna with F ventrieosus and I. seholastieuscontinues until the top of the Lamar Limestone. Compari-sons with the sequence in an outcrop about 1 km SE ofsection H, where the boundary between the Lamar Lime-stone and the post-Lamar / pre-Castile beds is exposed,have shown that the stratum typicum for F ventrieosus and I.seholastieus lies about 1 m below the top of the Lamar Lime-stone in this area. In this latter outcrop, near to section I ofORMISTON& BABCOCK, a brownish weathered chert is pre-sent near the top of the Lamar Limestone. Around thischert, in the limestones both the F ventrieosus-I. seholastieusradiolarian fauna and conodonts are common. The cono-dont fauna consists of Clarkina ehangxingensis italiea KOZUR,Clarkina n.sp. A, Clarkina n.sp. Band Hindeodus typiealis SWEET.In the post-Lamar/pre-Castile beds additionally Hindeodusjulfensis (SWEET), a characteristic (Upper) Dzhulfian -Changxingian conodont species, is present. The latterconodont fauna can be also found in the uppermost Altu-da Formation of the Glass Mountains (KOZUR, in press). Itis a Tethyan Dzhulfian fauna. The Dzhulfian age of theseconodonts is confirmed by the radiolarian fauna (seechapter IV).

ORMISTON & BABCOCK (1979) placed the F ventrieosus-I.seholastieusfauna in the Capitanian (upper part of Guadalu-pian Series), in agreement with the prevailing opinionabout the age of the Lamar Limestone. Only FURNISH(1973) regarded the Lamar Limestone as post-Capita-nian / pre-Dzhulfian.

As shown by KOZUR (in press) only the lower LamarLimestone with Yabeina lamarensis belongs surely to the Ca-pitanian, whereas the uppermost Lamar Limestone withthe F ventrieosus-I. seholastieus fauna belongs surely to theDzhulfian. The largest part of the Lamar Limestone be-tween these two horizons belongs either to the Capitanianor to the Dzhulfian (Wuchiapingian) depending from thefinal definition of the base of the Dzhulfian (Wuchiaping-ian) in the Asian Tethys.

3. Systematic partIf not otherwise indicated, the type locality of the new

species is the Torrente San Calogero section (locality S inText-Fig. 1), SW of the Pietra di Salomone, Sosio Valleyarea, Western Sicily (Italy).

Stratum typicum is the lower part of the predominantlyred upper Claystone Unit, sample 655 (Lower Dzhulfian).

The material with the repository number CK/ ... is depo-sited in the Dipartimento di Geologia e Paleontologia, Uni-versita di Palermo (Sicilia, Italia). The material with the re-

104

pository number N ... is deposited in the geology collec-tion of Museum of Northern Arizona, Flagstaff (Arizona,U.S.A.).

Radiolaria MÜLLER, 1858Polycystina EHRENBERG,1838Albaillellaria DEFLANDRE,1953emend. HOLDSWORTH,1969

Superfamily: Albaillellacea DEFLANDRE,1952Family: Follicucullidae

ORMISTON& BABCOCK,1979emend. KOZUR, 1981FollicucullinaeORMISTON& BABCOCK,1979Follicucullus ORMISTON & BABCOCKemend. KOZUR& MOSTLER,1989

Ty pes pee i es: Follieucullus ventrieosus ORMISTON& BAB-COCK,1979.

Rem ark s : KOZUR& MOSTLER(1989) emended Follieueullusand excluded forms, in which on the outer side the seg-mentation is not more visible, but they left "Follieueullus"monaeanthus ISHIGA& IMOTO,1982 in this genus. This spe-cies is a transitional form between the genera Parafol-lieueullus HOLDSWORTH& JONES, 1980 and Follieueullus OR-MISTON& BABCOCK, 1979. Its forerunner is Parafollieueulluseonvexus (RUDENKO& PANASENKO,1990).The so far known difference between Follieueullus andParafollieueullus is the presence of two lateral wings at thepseudothorax in all Parafollieueullus species and the ab-sence of these lateral wings in Follieueullus. "F" monaean-thus with only one wing at the pseudothorax is regardingto this feature equidistant to Parafollicueullus and Fol-lieueullus. If we continue to place this species in Follieueul-Ius then the original diagnosis of this genus has to beextended to include not only forms without lateral wingson the pseudothorax, but also forms with one lateralwing.The new investigations of the transition from Parafol-lieueullus in Follieueullus have shown that not only the later-al wings of Parafollieueullus, but also the pseudothorax ofthis genus is totally reduced and included in the largeapical cone of Follieueullus. The former pseudoabdomenof Parafollieueullus is by this transformed into the pseu-dothorax of Follieueullus (see under remarks to Parafol-lieueullus eonvexus). In "Follicueullus" monaeanthus the pseu-dothorax of Parafollieueullus is still present, but it may bealready totally reduced on the wingless side. Becausethe pseudothorax of "F" monaeanthus is homologous withthe pseudothorax of Parafollieueullus, but not homologouswith the pseudothorax of Follieueullus (homologous to theabdomen of Parafollieueullus, see above), "F" monaeanthus isby far closer related to Parafollieueullus than to Follieueullus.For this reason, this species is here placed into Parafol-lieueullus.Because the Follieueullus? eharveti-F porreetus of the Lepido-lina kumaensis fusulinid Zone (?) of Japan belongs prob-ably to the Dzhulfian (Araxoceratidae are present in thislevel), the genus Follieueullus begins near the base of theDzhulfian (or Wuchiapingian).

Follicucullus ventricosusORMISTON& BABCOCK,1979

(PI. 3, Fig. 13)1979 Follicucullus ventricosus n.sp. - ORMISTON & BABCOCK, p.

332-333, PI. 1, Figs. 6-14.


Dis tri but ion: Upper Permian of Circum-Pacific realmand West Texas. So far unknown from the Upper Permianof Western Sicily.

Rem ark s: Follicucullus ventricosus ORMISTON & BABCOCKhave been so far only reported from the Upper Permianof West Texas and Japan. The specie's was always cor-rectly determined; therefore no synonymy list is given.Both in West Texas and in Japan F ventricosus is a com-mon form. In Japan it occurs in the entire Upper Per-mian. Therefore its absence in the Eurasian Tethys andon the Philippines is difficult to explain.

Follicucullus bispinosus n.sp.(PI. 3, Figs. 10,11)

Der i vat ion 0 mi n is: According to the dorsal columellathat is bifurcated into two spines.

Holotype: The specimen on PI. 3, Fig. 10; rep.-no. N4062.

L 0 c u sty pic us: Outcrop at the SE side of the US High-way 62-180, 16 km WSW of its intersection with TexasRanch Road, 1108, Culberson County, West Texas.Western part of the Delaware Basin, about 7 km east ofthe reef, exposed in the Guadalupe Mts. Section H ofORMISTON& BABCOCK(1979).

S t rat um typ i cum: Light-gray weathered black lime-stone of the Lamar Limestone Member, Bell CanyonFormation. Thin bed about 10 cm below the top of theoutcrop. Lower Dzhulfian.

Mat e ria I : 23 specimens.Dia g nos is: Apical cone very large, straight, unseg-mented, but at its base sometimes with an indistinct,narrow ring. Pseudothorax large, elongated, inflated toa variable degree, along the dorsal side with a shallowsinus. Pseudoabdomen short, broad, somewhat ven-ralwards inclined. Aperture margin lobate in lateral view.Aperture elliptical in outline. Both free columellae areobliquely ventralwards directed. The ventral free col-umella is short, undivided. The dorsal free columella isvery long, in full preservation up to 5 times longer thanthe ventral columella. It bears one long outer spine. Theupper half of the dorsal columella is laterally broadened,the lower half is spine-like after the branching point ofthe outer spine. Within the test the columellae are totallyfused with the shell margin. They range upward until thelower half of the apical cone, but are often not visible intransmitted light, except in the pseudoabdomen, wherethey are mostly visible.

M easu rements:Length of apical cone = 159-172 /lomLength of pseudothorax = 98-120 /lomMaximum width of pseudothorax = 91-105 /lomLength of pseudoabdomen = 52-70 /lomMaximum width of pseudoabdomen = 111-120 /lom

Dis tri but ion: So far only known from the uppermostLamar Limestone Formation (Early Dzhulfian age) of thetype locality.

Rem ark s: Follicucullus ventricosus ORMISTON& BABCOCK,1979 has no outer spine on the outer free columella.

Follicucullus dilatatus RUDENKO, 1984(PI. 1, Figs. 4-6)

1983 Follicucullus ventricosusORMISTON& BABCOCK- SUYARI,KUWA-NO& ISHIDA,PI. 4, Figs. 6, (?)7,non! Fig. 10.

1984 Fotlicucutlus dilatatus RUDENKO,sp.nov. - BELJANSKIJ,NIKITINA& RUDENKO,p. 54-55, PI. 8, Figs. 6, 7.

1984 Follicucullus lagenarius RUDENKO,sp.nov. - BELJANSKIJ,NIKITI-NA& RUDENKO,p. 55, PI. 8, Fig. 11.

Mat e ria I : Several1 000 specimens.Dia g nos is: Apical cone unsegmented, slightly curvedor straight. Pseudothorax distinctly inflated, longer thanbroad, subcylindrical. Pseudoabdomen indistinct ormissing. Distal free columella ventralwards curved, onlyrarely preserved.

M easu rements:Length of apical cone = 130-159 /lomLength of pseudothorax = 112-141 /lomMaximum width of pseudothorax = 94-106 /lom

Dis tri but ion: Uppermost "Midian" Stage (uppermostCapitanian or lowermost Dzhulfian s.l.) of Primorje area(SE Siberia). Dzhulfian of Sosio Valley. Upper DzhulfianNeoalbaillella ornithoformis Zone of Japan in the openoceanic fauna.

Rem ark s: In Follicucullus lagenarius RUDENKO, 1984 thepseudothorax is more abruptly separated from the apic-al cone than in F dilatatus RUDENKO, 1984. However, alltransitional forms are present between these two spe-cies in Sicily. Both in Siciliy and in the Sichote Alin bothspecies occur together in the same samples. F lagenariusis therefore regarded as synonym of F dilatatus (both spe-cies are figured in the same paper, F dilatatus has pagepriority and the type material is better preserved than inF lagenarius). Internal molds of F dilatatus have always thecharacter of F lagenarius.Follicucullus ventricosus ORMISTON& BABCOCK, 1979 has ashort, but distinct pseudoabdomen, the apical cone isalways straight, and it displays a low, ring-like segmentat its base.Follicucullus porrectus RUDENKO, 1984 with short, but dis-tinct pseudoabdomen is similar, but the pseudothorax isnot so wide.

Follicucullus porrectus RUDENKO, 1984(PI. 1, Figs. 7-11)

1980 Follicucullus scholasticusORMISTON & BABCOCK,pars. -ISHIGA& IMOTO,p. 340, PI. 4, only Figs. 5-7.

1982 Follicucullus scholasticus ORMISTON& BABCOCK- ISHIGA,KITO& IMOTO,PI. 2, Figs. 8-10.

1983 Follicucullus scholasticus ORMISTON& BABCOCK,pars. - Su-YARI,KUWANO& ISHIDA,PI. 3, Figs. 1, (?)2, 3-5, 7, (?)8, non! Figs. 6,9.

?1983 Follicucullus ventricosus ORMISTON& BABCOCK,pars. - Su-YARI,KUWANO& ISHIDA,PI. 4, Fig. 10, non! Figs. 6,7.

1984 Follicucullus porrectus RUDENKO,sp.nov. - BELJANSKIJ,NIKITI-NA& RUDENKO,p. 55-56, PI. 8, Figs. 3, 10.

1984 Follicucullus scholasticus ORMISTONet BABCOCK,1979. -BELJANSKIJ,NIKITINA& RUDENKO,p. 54, PI. 8, Figs. 4,5.

1984 Follicucullus scholasticus ORMISTON& BABCOCK,morphotypeII, pars. -ISHIGA, PI. 1, only Figs. 2-4, (?)5, (?)6.

1985 Follicucullus scholasticus ORMISTON& BABCOCK,morphotypeII, pars. - ISHIGA,p. 180, PI. 1, Figs. 22-28, PI. 2, Figs. 2,3, non (?) Figs. 1, 4 (perhaps strongly deformed Follicucul-Ius porrectus n.sp.).

1985 Follicucullus scholasticus ORMISTON& BABCOCK,pars. - NAKA& ISHIGA,PI. 1, Figs. 1, (?)2, 5, 7, non! Figs. 3, (?)4, (?)6.

1985 Follicucullus scholasticus ORMISTON& BABCOCK,pars. - ISHI-DA,PI. 1, Fig. 6, non (!) Fig. 5.

1985 Follicucullussp. cf. scholasticusORMISTON & BABCOCK,pars.-WAKITA,Figs. 3/1, (?)3/2, non! Figs. 3/4,3/5.

1985 Follicucullus ventricosus ORMISTON& BABCOCK- WAKITA,Fig.3/4.

1985 Follicucullus scholasticus ORMISTON& BABCOCK- SASHIDA&TONISHI,PI. 7, Figs. 1,3.

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? 1986 FollieuGUllus seholastieusORMISTON & BABCOCK, 1979. -ISHIGA& MIYAMOTO,p. 330-331, PI. 64, Figs. 9-11.

1986 FollieuGUllus seholastieus ORMISTON& BABCOCK, morphotypeII (in the plate explanations erroneously designated asmorphotype I). - ISHIGA, WATASE & NAKA, p. 129, PI. 2,Figs. 12-16, (?)17-19.

1987 FolliGUeullus seholastiGUsORMISTON& BABCOCK, morphotypeIIISHIGA - NISHIMURA& ISHIGA, PI. 1, Figs. 4-6.

? 1987 FolliGUeullus seholastieus ORMISTON& BABCOCK, morphotypeIIISHIGA (1984), pars. - PILLAI & ISHIGA, PI. 1, only Fig. 10.

1988 FolliGUeullus seholastieus ORMISTON& BABCOCK (morphotype1 sensu ISHIGAet aI., 1986). - OE WEVER, BOURDILLON-DEGRISSAC& BECHENNEC,Fig. 2A.

1989 FolliGUeullus n.sp. (Follieueullus seholastiGUs, morphotype IIsensu ISHIGA). - CATALANO,01 STEFANO& KOZUR, Fig. 6 O.

1991 FollieuGUllus japoniGUs ISHIGAn.sp. -ISHIGA, p. 108-111, P11,Figs. 1-15; PI. 2, Fig. 1.

1992 Ishigaeonus n.sp. (= FolliGUeullus seholastieus, morphotype IIsensu ISHIGA, 1985). - CATALANO, 01 STEFANO & KOZUR,Fig. 6 L.

Mat e ria I: Severa110.000 specimens.Dia g nos is: Test slender conical, also on the outer testsurface clearly subdivided in apical cone, pseudothoraxand pseudoabdomen. Apical cone long, unsegmented,straight or slightly curved, sometimes oblique. Pseu-dothorax, narrow, but distinctly broader than remainingtest. Pseudoabdomen short to moderately long, situ-ated mostly somewhat obliquely to the pseudothorax.

Measurements:Length of the apical cone = 110-200 !J..mLength of pseudothorax = 80-141 !J..mMaximum width of pseudothorax = 83-94 !J..mLength of pseudoabdomen = 59-100 !J..m

Dis tri but ion: (?) Lepido/ina kumaensis fusulinid Zone (Up-per Capitanian or Lower Dzhulfian / Lower Wuchiaping-ian) of Japan and time-equivalent beds of Sichote Alin(SE-Siberia), Dzhulfian s.str., (?) Changxingian of Japan,Upper Permian of Oman and Sicily.

Rem ark s: Despite of the huge amounts of specimens inthe Sicilian material, no forms with preserved free col-umellae are present. Also in most of the Japanesematerial, the free columellae are broken away. Only ISHI-GA (1991) published well preserved material, in whichboth free columella are mostly preserved. If they arepresent, both the dorsal and ventral free columella areobliquely ventralwards directed.Fo//ieueu//us porree/us RUDENKO, 1984 corresponds to Fseho/astieus, morphotype II sensu ISHIGA, 1984. However,this species is closer related to F venlrieosus ORMISTON&BABCOCK, 1979 than to /shigaeonus seho/astieus ORMISTON&BABCOCK, 1979. It was described by ISHIGA(1991) as Fo/-/ieueullus japonicus n.sp. that is a junior synonym of F por-rectus RUDENKO, 1984. The holotype of F porreelus is aslender form with rather long pseudoabdomen. But it fitsinto the intraspecific variability, shown in the well pre-served material by ISHIGA(1991). The paratype is a typic-al specimen. The rather big intraspecific variability canbe also confirmed in the Sicilian material. However, Fjaponieus ISHIGA,var. A and var. B do not belong to F porree-Ius RUDENKO.Slender representatives of F venlrieosus are very similar,but their pseudothorax is broader than in F porreelus andthe likewise broader pseudoabdomen is more obliquelyarranged. Sometimes slender specimens of F venlrieosushave been included in Fo//ieueu//us seho/aslieus, morpho-type II./shigaeonus seho/aslieus ORMISTON & BABCOCK displays aslender conical test that is on its outer surface undi-vided.

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Whereas all previous authors placed F porrectus into Fseho/astieus, morphotype II, DEWEVERet al. (1988) placedthis species into F seho/aslieus, morphotype I. However,ISHIGA(1984) and all other previous authors designatedall forms that correspond to the holotype of F seho/aslieusORMISTON& BABCOCK as morphotype I. Only in ISHIGA,WATASE& NAKA (1986) F seho/aslieus, morphotype II was inthe plate explanation erroneously designated by a print-ing mistake as morphotype I, but in the text of this paperboth morphotypes have been correctly designated.

Genus: Parafol/icucu/lusHOLDSWORTH & JONES, 1980

Ty pes p e ci es: Parafo//ieueu//us fusiformis HOLDSWORTH&JONES, 1980

Parafollicucullus monacanthus(ISHIGA & IMOTO, 1982)

(PI. 1, Fig. 23)1980 FollieuGUllus sp. A - ISHIGA & IMOTO, p. 340, PI. 4, Figs.

11-15.1982 b Follieueullus monaeanlhus ISHIGA& IMOTOn.sp. -ISHIGA, KITO&

IMOTO,p. 276-277, PI. 4, Figs. 15-19.1990 Follieueullus monaeanthus ISHIGA& IMOTO- GRAPES, LAMB et aI.,

Fig.69.

Mat e ria I: One reworked specimen in sample 655 amonghuge amounts of Upper Permian radiolarians.

Dis tri but ion: Guideform for the Capitanian of Japan.The single specimen in the Dzhulfian of Western Sicily issurely reworked. This species indicates the presence ofpelagic Capitanian in Western Sicily that has been so farnot found in outcrops. Most probably, it consists of graypelagic claystones, like the underlying Wordian and theoverlying lowermost Dzhulfian.

Rem ark s: The new assignment of P. monaeanthus (ISHIGA&IMOTO)to the genus Parafo//ieueu//us is discussed underthe remarks to the genus Fo/lieueu//us. The relation to Para-fo//ieueu//us postfusiformis n.sp. is discussed under thisspecies.

Parafollicucullus convexus(RUDENKO & PANASENKO, 1990)

(PI. 1, Fig. 20)

1987 Pseudoalbaillella sp. cf. P fusiformis (HOLDSWORTH& JONES),pars. - NISHIMURA& ISHIGA, p. 176-177, PI. 1, only Fig. 14.

1988 FollieuGUllus monaeanthus ISHIGA & IMOTO, 1980. - OE WEVER,BOURDILLON-DEGRISSAC& BECHENNEC,Fig. 2 O.

1989 ParafolliGUeultus n.sp. - KOZUR in CATALANOet aI., Fig. 6 H.1990 Pseudoalbaillella eonvexa RUDENKO et PANASENKO, sp.nov. -

RUDENKO& PANASENKO,p. 184, PI. 18, Figs. 6,7.

M a teri a I: 4 specimens.Dia g nos is: Apical cone long, mostly a little curved.Pseudothorax small, globular, with two short wings. Thepseudoabdomen consists of a long, narrow neck with-out a ring-like, short segment, followed bya bottle-liketo ellipsoidal part that is considerably broader than theneck. The last segment is short, a little ventralwards in-clined. Dorsal and ventral free columellae short,obliquely ventralwards directed. Aperture at the lowerend oval.


M easu rem ents:Length of apical cone = 100-170 J.LmLength of pseudothorax = 41-63 J.LmMaximum width of pseudothorax = 58-70 J.LmLength of pseudoabdomen = 176-280 J.LmWidth of neck (minimum width of pseudoabdomen) =47-64 J.LmMaximum width of pseudoabdomen = 106-120 J.Lm

Dis tri but ion: Capitanian, (?) Wordian. In Western Sicilyand Oman very rare reworked (?) forms occur in LowerDzhulfian deposits. In sequences of Japan this speciesoccurs above the Wordian Parafo//icucu//us fusiformisHOLDSWORTH& JONESand below the Capitanian Parafo/-Iicucullus monacanlhus (ISHIGA & IMOTO). In Primorje (SE-Siberia) P convexus occurs in the lowermost part of theCapitanian P monacanlhus fauna.

Rem ark s: The few (?) reworked specimens of the Sici-lian material are badly preserved. The upper part of theapical cone and the distal part of the test are alwaysbroken away. However, the diagnostic most importantpart, the small globular pseudothorax with its twowings, the following long, narrow neck without a ring-like segment and the following bottle-like part of thepseudoabdomen are always preserved.Parafollicucullus fusiformis HOLDSWORTH& JONES, 1980 isdistinguished by a distinct, narrow, ring-like segment onthe shorter and not so narrow neck. Most similar to Pconvexus are specimens of P fusiformis with long, narrowneck, figured by TAZAWA et al. (1984). However, alsothese forms have a distinct, ring-like narrow segment inthe middle part of the neck.It is not sure, whether P convexus has evolved directlyfrom P fusiformis. Together with P fusiformis, but also be-fore the first occurrence of this species, there occurforms, that NISHIMURA& ISHIGA (1987) placed togetherwith P convexus in Pseudoa/baillella sp. cf. P fusiformis (NI-SHIMURA& ISHIGA, 1987, PI. 1, Figs. 16-18). These formshave a broader, shorter neck than P convexus, but alsowithout narrow segment in the middle part of the neck.They are very similar to Parafollicucullus nanjingensiSHENG &WANG, 1985, which is only distinguished by the widerand shorter segment after the neck. May be, that P nan-jingensis is the forerunner of P convexus (through transi-tional forms, like P sp. cf. P fusiformis sensu NISHIMURA&ISHIGA,1987, PI. 1, Figs. 16-18).Parafollicucullus monacanlhus (ISHIGA& IMOTO,1982) evolvedfrom P convexus by disappearance of one wing on thepseudothorax. Simultaneously, the pseudothorax isstrongly reduced and only at the wing side still hemi-globular. The other side of the pseudothorax is often al-ready inseparable from the apical cone. Simultaneouslywith total disappearance of the wings also the pseu-dothorax disappears and the former neck (upper part ofthe pseudoabdomen), the former pseudothorax and theapical cone of Parafollicucullus are transformed into a sin-gle apical cone of Follicucullus. Therefore the lower bigpart of the pseudoabdomen in Parafollicucullus convexusand P monacanlhus is transformed into the pseudothoraxof typical Follicucullus.In well preserved material of Follicucullus venlricosus (typespecies). the former pseudothorax of Parafollicucullus isvisible in transmitted light within the lower part of theapical cone. Even the narrow ring of the neck betweenthe pseudothorax and pseudoabdomen of Parafollicucu/-Ius fusiformis is still present in Follicucullus venlricosus andsituated there at the base of the apical cone, a further

evidence that the pseudothorax and the following neckof Parafollicucullus were transformed into the apical coneof Follicucullus.The pseudothorax of Follicucullus is therefore not homo-logous to the pseudothorax in Parafollicucullus. For thisreason "Follicucullus" monacanthus with Parafollicucullus-pseudothorax is here placed in Parafollicucullus (see alsoremarks to the genus Follicucullus). It is a transitional formto Follicucullus (beginning reduction of the wings and ofthe Parafollicucullus-pseudothorax), but all the main cha-racters of the genus Parafollicucullus are still present andno feature of the real Follicucullus (absence of Parafo/-/icucullus-pseudothorax, absence of lateral wings, trans-formation of the lower part of the Parafollicucullus-pseu-doabdomen into the Follicucullus-pseudothorax) is alrea-dy present.In continuation of this development, in the most ad-vanced Follicucullidae the whole outer segmentationdisappeared or is only very indistinct.DE WEVER, BOURDILLON-DEGRISSAC& BECHENNEC(1988)placed Parafollicucullus convexus into "Follicucullus" monacan-thus ISHIGA & IMOTO, 1980. This species, however, hasbeen only established in 1982. Moreover, the specimen,figured as "F" monacanlhus by DE WEVERet al. (1988) dis-plays a well developed globular pseudothorax (unre-duced on both sides) with the proximal part of twobroken away lateral wings. This form has nothing to dowith P monacanlhus.The presence of Parafollicucullus convexus in Oman within atypical Upper Permian association with Follicucullus por-reclus n.sp. and /shigaconus scho/asticus (ORMISTON& BAB-COCK) is insofar important, as this species may reallyrange into the Upper Permian. However, DEWEVERet al.(1988) have not given any sample data and any dataabout the distribution of the Permian radiolarians ofOman. Therefore it is not clear, whether the figured ra-diolarians have been derived from the same bed. Be-cause only one sample (FB 703) is mentioned, all 3figured forms by DE WEVERet al. (1988) may have beenderived from a single sample. In this case, the Capita-nian P convexus may range upward (with few specimens)into the Dzhulfian or also in Oman reworking of MiddlePermian radiolarians into Upper Permian radiolarianfaunas occurs.

Genus: PseudoalbaillellaHOLDSWORTH & JONES, 1980

Ty pes p e ci es: Pseudoa/baillella sea/praIa HOLDSWORTH&JONES

Pseudoalbaillella eurasiaticaKOZUR, KRAHL & MOSTLER, 1989

(PI. 1, Figs. 21, 22)

1982 a Pseudoa/baillella sp. aft. Ps. longieornis ISHIGA& IMOTO-ISHIGA,KITO& IMOTO,PI. 3, Fig. 11.

1982 b Pseudoalbaillella sp. aft. Ps. longicornis ISHIGA& IMOTO-ISHIGA,KITO& IMOTO,p. 75, PI. 2, Figs. 1-4, 6, non! Figs. 5, 7.

1987 Pseudoalbaillella cf. eurasiatiea KOZUR, KRAHL & MOSTLER inKOZUR & MOSTLER (im Druck). - KOZUR & KRAHL, p. 363,Figs.4-6.

1989 Pseudoatbailtella (Pseudoalbaillella) eurasiatiea KOZUR, KRAHL &MOSTLERn.sp. - KOZUR& MOSTLER, p. 177-178.

1989 Pseudoalbaillella eurasiatiea KOZUR, KRAHL & MOSTLER- KOZURin CATALANOat aI., Fig. 6 F.

1990 Pseudoalbaillella aft. P. longieornis ISHIGAand IMOTO- Tu MAN-DA,SATO& SASHIDA, PI. 1, Fig. 4.

107


1991 Pseudoalbaillella eurasialica KOZUR, KRAHL & MOSTLER - CATA-LANO, 01 STEFANO & KOZUR, PI. 6, Fig. 5.

1992 Pseudoalbaillella eurasialica KOZUR, KRAHL & MOSTLER - CATA-LANO, 01 STEFANO & KOZUR, Fig. 6 I.

Material: 18specimens.Dis tri but ion: Wordian (Middle Permian) to Dzhulfian(Upper Permian) of Japan, Philippines, Crete (Greece)and Sicily.

Rem ark s : Representatives of P eurasiaticus KOZUR, KRAHL& MOSTLERwith short pseudoabdomen have been re-ported from undoubtedly Dzhulfian radiolarian associ-ations of Japan. Therefore such forms may belong to theautochthonous components of the Dzhulfian radiolarianfaunas of Sicily.Representatives with long pseudoabdomen (PI. 1,Fig. 21) are surely reworked, because such forms arecharacteristic for the Wordian and lower Capitanian ofthe Eurasian Tethys.

Genus: IshigaconusKOZUR & MOSTLER, 1989

Ty pes p e ci es: Follicucullus scholasticus ORMISTON& BAB-COCK,1979

Ishigaconus scholasticus(ORMISTON & BABCOCK, 1979)(PI. 1, Figs. 1-3; PI. 3, Figs. 9, 12)

1979 Follicucullus scholaslicus n.sp. - ORMISTON & BABCOCK, p.333-334, PI. 1, Figs. 1-5.

1989 Ishigaconus scholaslicus ORMISTON & BABCOCK - KOZUR &MOSTLER, p. 181-182.

Mat e ria I : Several1 000 specimens.Dis tri but ion: Topmost Lamar Limestone of the Gua-dalupe Mountains (according to KOZUR, in press, ofDzhulfian age), Upper Permian of Japan, Philippines,Oman and Western Sicily.

Rem ark s: Ishigaconus scholasticus (ORMISTON& BABCOCK)have been reported in numerous papers from the wholeCircum-Pacific realm, but also from Western Sicily and(type material) from West Texas. This easily determin-able species was always correctly determined. There-fore only the original description and the change of thegenus assignment is quoted in the reference list.Often Follicucullus porrectus RUDENKO,1984 was placed in-to "Follicucullus" scholasticus as well, but since ISHIGA(1984)mostly separated as morphotype II (see synonymy list ofFollicucullus porrectus).Ishigaconus bipartitus (CARIDROIT& DEWEVER, 1984) is eas-ily to distinguish by its strongly curved apical cone. Ac-cording to ISHIGA& MIYAMOTO(1986) "Follicucullus" hamatusCARIDROIT& DEWEVER, 1984 is a synonym of "F" bipartitusCARIDROIT& DE WEVER, 1984, representing the isolatedupper half of this species. This view is accepted in thepresent paper.Ishigaconus furcus (CARIDROIT& DEWEVER, 1986) n. corr. isdistinguished by the second spine on the dorsal freecolumella. Because the free columella are rarely fullypreserved, the separation of these two species is dif-ficult. The subdivision of the shell into two halfs re-garded by CARIDROIT& DEWEVER(1986) as characterist-ic feature of "F" furcus, is also present in I. scholasticus (seeORMISTON& BABCOCK, 1979, PI. 1, Figs. 3-5 and present

108

paper, PI. 1, Fig. 2). This feature is especially well visiblein slightly corroded specimens.As pointed out by ORMISTON& BABCOCK (1979, p. 333),the dorsal free columella is not fully preserved in anyspecimen of the type series of Ishigaconus scholasticus.Therefore it was uncertain, whether the dorsal free col-umella of I. scholasticus has a second outer spine, as in I.. furcus, or not. Re-investigations of excellently preservedmaterial from the type locality have shown, that the se-cond spine on the dorsal columella is also absent in spe-cimens with fully preserved dorsal columella. ThereforeIshigaconus furcus (CARIDROIT& DEWEVER) is an independ-ent species.

Genus: Cariver n.gen.

Derivat ion om i n is: Combined from CARIDROITand DEWEVER, in honour of the authors of the type species

Ty pes p e ci es: Follicucullus orthogonus CARIDROIT & DEWEVER,1984

Dia g nos is: Apical horn long, unsegmented. Pseu-dothorax large, inflated. Pseudoabdomen, partly alsoposterior part of pseudothorax ventralwards curved.Aperture oval, situated on the ventral side, perpendicu-larly or nearly perpendicularly to the test axis. A ventralsinus on the pseudothorax is always present, a dorsalsinus may be additionally present.

Assigned species:Follicucullus orthogonus CARIDROIT& DEWEVER, 1984 Cariverdorsoconvexus n.sp.Cariver n.sp. A (= Follicucullus sp. aft charveti sensu CARI-DROIT& DEWEVER, 1986).Carivern.sp. B (= Follicucullus sp. aft. orthogonussensu CARI-DROIT& DEWEVER, 1986).

Dis tri but ion: Circum-Pacific realm and Western Sicily.Restricted to the Upper Permian (Dzhulfian).

Rem ark s: In Follicucullus ORMISTON& BABCOCK, 1979 theaperture is always situated at the lower end of the test.Typical representatives of Follicucullus display a dorsal,but no ventral sinus in the pseudothorax.Follicucullus ? charveti CARIDROIT& DE WEVER, 1984 is theforerunner of Cariver n.gen. and a transitional form be-tween Follicucullus and Cariver. The pseudoabdomen of F?charveti is mostly clearly inclined towards the ventral sideand the aperture is mostly situated obliquely to the testaxis towards the ventral side. A distinct ventral sulcus ispresent in the pseudothorax, like in all Cariver species.Unfortunately, the taxonomic importance of the pres-ence of a ventral sulcus is unknown. If the presence of aventral sulcus in the pseudoabdomen would be a taxo-nomically important feature, then F? charveti CARIDROIT&DEWEVER, 1984 and F ? falx CARIDROIT& DEWEVER, 1984should be placed into the genus Carivern.gen.By development of a strongly curved pseudoabdomenwith ventrally situated aperture (perpendicularly to thetest axis), Cariver n.sp. A developed from F ? charveti.ISHIGA & MIYAMOTO (1986) regarded Cariver orthogonus(CARIDROIT& DE WEVER, 1984) as morphotype of Fol-licucullus? charveti CARIDROIT& DEWEVER, 1984. However,the two forms that were figured as F ? charveti, morpho-type orthogonus are transitional forms from F ? charveti toCariver n.sp. A (ISHIGA& MIYAMOTO,1986, PI. 64, Fig. 5) orinto Carivern.sp. B (PI. 64, Fig. 4). In these specimens thepseudoabdomen is clearly curved toward the ventral


side and the aperture lies obliquely to the test axis. Thisis also the case in all other forms, figured by ISHIGA&MIYAMOTO(1986) under Follicucullus charveti, only the de-gree of the bent of the pseudoabdomen is variable, likein the type series of F ? charveti.The drawing of F? charveti by CARIDROIT& DE WEVER(1984) with an aperture at the lower end of the test (incontinuation of the test axis) is rather misleading com-pared with the photographs of the type material. Thematerial published by ISHIGA& MIYAMOTO(1986) is by farbetter preserved than the type material of F ? charveti,published by CARIDROIT& DE WEVER(1984). It showsclearly the transition character of F ? charveti betweenFollicucullus and Cariver.F ? charveti begins in the latest Capitanian or earliestDzhulfian (?) Lepidolina kumaensis Zone of Japan, whereasthe typical Cariver species, including Cariver orthaganus(CARIDROIT& DEWEVER,1984), began later, in undoub-tedly Upper Permian deposits.

Cariver dorsoconvexus n.sp.(PI. 1, Figs. 15-17,19)

1989 Follicucullus ? n.sp. aft. charveti CARIDROIT & DE WEVER -KOWR in CATALANO et aI., Fig. 6 K.

1992 Highly evolved representative of the Follicucullidae (n.gen.,n.sp.). - CATALANO, 01 STEFANO & KOZUR, Fig. 6 K.

Der i vat ion 0mi n is: According to the strongly convexdorsal margin of the pseudothorax and pseudoab-domen.

Hol 0 typ e: The specimen on PI. 1, Fig. 16; rep.-no CK/111-64

Mat e ria I: Several1 00 specimens.

Dia g nos is: Apical horn long, straight or insignificantlycurved. Pseudothorax large, inflated, inclined towardsthe dorsal side. Its dorsal margin is strongly convex anddisplays in well preserved specimens a shallow sulcus(PI. 1, Fig. 15). The ventral margin is also convex and dis-plays a broad, deep sulcus. The pseudoabdomen islong, strongly ventralwards curved. The oval aperture issituated in fully preserved specimens on the ventralside, perpendicularly (or nearly so) to the test axis. Thedorsal margin of the pseudoabdomen is strongly con-vex, the ventral margin straight to slightly concave.

M easu rements:Length of apical horn = 106-129 J.1m.Length of pseudothorax = 88-127 J.1m.Maximum width of pseudothorax = 82-94 J.1m.Length of pseudoabdomen = 59-71 J.1m.

Dis tri but ion: Dzhulfian of Sosio Valley area, WesternSicily.

Rem ark s: Cariver dorsoconvexus n.sp. is characterized byits strongly convex dorsal margin of pseudothorax andpseudoabdomen. This is mainly caused by a dorsalwardbent of the pseudothorax before the ventralwards bentof the pseudoabdomen. No other Cariver species showsa dorsalward bent of the pseudothorax. In contrast, atleast the distal part of the pseudothorax is in differentdegree ventralwards curved or inclined in the other Cariv-erspecies.

Genus: Lacisus n.sp.Der i vat ion 0mi n is: Arbitrary composition of letters.

Ty pes p e ci es: Lacisus siphunculus n.gen. n.sp.

Dia g nos is: Test slender, smoking-pipe-shaped. Apicalcone very long, unsegmented. Pseudothorax elongatedellipsoidal, rather narrow, but distinctly broader than ap-ical cone and pseudoabdomen. The long pseudoabdo-men is in its apical part straight, in the following partcurved perpendicularly or nearly perpendicularly to thetest axis. Distal part of pseudoabdomen widened. Aper-ture round, situated on the ventral side, perpendicularly(or nearly so) to the test axis.The inner structure of the pseudothorax and pseudoab-domen consists of densely spaced narrow rings (trabe-cles ?) that connect the two columellae. In slightly cor-roded specimens, this structure is seen also externally.

Dis tri but ion: Until now only known from the Dzhulfianof the Sosio Valley area, Western Sicily.

Assigned species:Lacisus siphunculus n.gen. n.sp.Lacisus n.sp.

Rem ark s: Ishigaconus KOZUR& MOSTLER,1989 displays nolong pseudoabdomen curved perpendicularly ventral-wards against the test axis.Cariver n.gen. displays a considerably broader pseu-dothorax and a laterally compressed pseudoabdomenwith oval aperture. Cariverhas only very few trabecles onthe ventral side that do not reach the dorsal side.

Lacisus siphunculus n.gen. n.sp.(PI. 1, Figs. 12-14)

Derivatio nominis: According to the shape of thetest.

Hol 0 typ e: The specimen on PI. 1, Fig. 12; rep.-no. CK/1188 VI-33.

Mat e ria I: Several1 00 specimens.

Dia g nos is: Apical cone very long, straight, unsegmen-ted. Pseudothorax elongated-ellipsoidal, long, withgradual transition to both apical cone and pseudoab-domen. The narrow, densely spaced rings between thedorsal and ventral columellae are especially well deve-loped in the distal half of the pseudothorax. Pseudoab-domen long, strongly curved, distal part situated per-pendicularly (or nearly so) to the test axis. The distal partof the pseudoabdomen is strongly widened and oftensomewhat wider than the pseudothorax. Apertureround, situated on the ventral side of the test, perpen-dicularly (or nearly so) to the test axis.

M easu rements:Length of apical cone = 108-147 J.1m.Length of pseudothorax = 118-147 J.1m.Maximum width of pseudothorax = 71-82 J.1m.Length of pseudoabdomen = 129-165 J.1m.Distal diameter of pseudoabdomen = 71-85 J.1m.

Dis tri but ion: Only known from the Dzhulfian of the So-sio Valley area.

Rem ark s: Lacisus n.sp. (PI. 1, Fig. 18) displays a sigmoid-ally bent test. The pseudothorax of this species is only alittle wider than adjacent parts of the test.

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Genus:

Genus:

Family:

Family:

Suborder:Superfamily:

Spumellaria EHRENBERG,1875Actinommacea HAECKEL,1862emend. KOZUR& MOSTLER,1979PraeconocaryommidaePESSAGNO,1976PhaenicosphaeraHAECKEL,1887

Ty pes p e ci es: Carposphaera nodosa HAECKEL

Urocyrtis ? sp.(PI. 2, Fig. 2)

Rem ark s: This species is very similar to Urocyrtis PAN-TANELLIthat is, however, only known since the Norian. Incontrast to Urocyrtis, the distal tube ends in a (? solid) partwithout pores. However, in some Upper Triassic Urocyrtisthe tubus may be terminally closed and its distal parthas so small pores that it looks poreless in recrystallizedspecimens.Unfortunately, the inner features of the Upper Permianforms are unknown. Their generic assignment is there-fore unsure, but it is very probable that these forms be-long to the Nassellaria.

Nassellaria EHRENBERG,1875EucyrtideaceaEHRENBERG,1847SyringocapsidaeFOREMAN,1973UrocyrtisPANTANELLI,1880 emend.

Ty pes p e c i es: Urocyrtis amaliae PANTANELLI,1880Synonyma: Syringocapsa NEVIANI, 1900; Gigi DE WEVER,1982

Em end e d dia g nos is: Slender elongated proximalpart with 1-3 small segments, on the outer surface notclearly separated from each other. Apical horn oftenpresent. The distal segment is very large, globular or alittle ellipsoidal. It bears a moderately to very long hol-low tubus with mostly large pores. Test wall with pores.

Rem ark s: All Urocyrtis species (including the later desig-nated type species U. amaliae PANTANELLI,1880), estab-lished by PANTANELLI(1880), displayaslender elongatedapical part, built up of one-two segments (outside most-ly not separated by constrictions) and a big globular toslightly ellipsoidal distal segment that ends in a verylong, narrow, hollow distal tubus. No spines are presentat the large segment.The same structure displays Theosyringium robustumVINAS-SA DEREGNY, 1900, the type species of Syringocapsa NE-VIANI, 1900. Only the distal tubus is considerably shorterin this species. But the length of the distal tubus is highlyvariable in this group. Moreover, if the distal tubus is verylong, it is often not preserved in its fuillength.The genus Gigi DE WEVER, 1982 has a very long distaltubus, like the type species of Urocyrtis. No differencesare recognizable between Gigi DE WEVER, 1982 and Uro-cyrtis PANTANELLI, 1880. Therefore also Gigi DE WEVER,1982 is a junior synonym of Urocyrtis PANTANELLI,1880.

Suborder:Superfamily:

Mostlerispongus n.gen.

Ty pes p e c i es: Mostlerispongus sosioensis n.gen. n.sp.Deriva ti 0 nom i n is: In honoJ.lr of Prof. Dr. H. MOSTLER,lnnsbruck.

Dia g nos is: Spongy shell globular to slightly ellipsoidal,with 6 spongy, short round arms with the same diameterthroughout their length. These arms are arranged in 3axes, perpendicularly to each other. All arms end in aterminal, basally carinate spine of round cross section.

Assigned species:Mostlerispongus sosioensis n.gen. n.sp.

Dis tri but ion: Dzhulfian of Western Sicily. Upper Per-mian of Philippines.

Rem ark s: Hexaporobrachia KOZUR & MOSTLER, 1979 isdouble-walled and has coarse outer pore frames.

Mostlerispongus sosioensis n.sp.(PI. 2, Fig. 5)

Der i vat ion 0mi n is: According to the occurrence in theSosio Valley area.

Holotype: The specimen on PI. 2, Fig. 5; rep.-no CK/111-65.

M ateri al: 7 specimens.Diagnosis and distribution: As for the genus.Measurements:Diameter of shell = 150-277 /lom.Length of arms = 118-161 /lom.Diameter of arms = 71-123 /lom.

Rem ark s: The figured specimen from the Busuanga Is-land, Philippines (TUMANDA,TADASHI& SASHIDA, 1990) islarger than the material of Western Sicily, but otherwiseidentical. The measurements of this specimen weretaken into consideration in the above measurements.

Family: HexaporobrachiidaeKOZUR& MOSTLER,1979

Hindeosphaera ? n.sp.(PI. 2, Fig. 3)

Rem ark s: By the presence of a single main spine andnumerous by-spines this very rare form is similar to theTriassic Entactinaria genus Hindeosphaera KOZUR& MOST-LER, 1979. However, it is considerably smaller and theinner structures are unknown. There are also somemorphological similarities to Jurassic and CretaceousNassellaria.

Suborder: EntactinariaKOZUR& MOSTLER,1982

Superfamily: PalaeoscenidiaceaRIEDEL,1967

Family: HindeosphaeridaeKOZUR& MOSTLER,1981

Genus: HindeosphaeraKOZUR& MOSTLER,1979

Ty pes p e ci es: Hindeosphaera foremanae KOZUR& MOSTLER,1979

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•

Rem ark s: The genus Phaenicosphaera HAECKEL is a veryconservative taxon, present at least since the LowerPermian. Several genera have been established for thistaxon. At least the Upper Paleozoic and Mesozoicgenera are inseparable from each other, but also the Re-cent Phaenicosphaera cannot be separated at the presentstage of our knowledge from these Upper Paleozoic -Mesozoic forms.NAZAROV& ORMISTON(1985) introduced the new genusHegleria without any discussion of similar Mesozoic andCenozoic genera that have been established for theseforms since the last century.I agree with SHENG& WANG (1985) that all these simpleforms with mammae and 2-3 medullary shells, con-nected to each other by numerous spines, should beplaced in Phaenicosphaera HAECKEL. At least Hegleria NA-ZAROV& ORMISTON(1985) is inseparable from the Trias-sic-Upper Cretaceous Praeconocaryomma PESSAGNO,1976that was seemingly unknown to NAZAROV& ORMISTON(1985).

Phaenicosphaera mammifera(NAZAROV & ORMISTON, 1985)

(PI. 2, Fig. 1)

1985 Hegleria mammifera NAZAROV & ORMISTON, n.sp. - NAZAROV &ORMISTON, p. 22-23, PI. 6, Figs. 3-5.

1989 Phaenicosphaera mammifera (NAZAROV & ORMISTON). - KOZUR inCATALANO et aI., Fig. 61.

1991 Phaenicosphaera mammifera (NAZAROV & ORMISTON). - CATALANO,01 STEFANO & KOZUR, PI. 6, Fig. 6.

1992 Phaenicosphaera mammifera (NAZAROV & ORMISTON). - CATALANO,01 STEFANO & KOZUR, Fig. 6 J.

Mat e ria I: Several1000 specimens.Dis tri but ion: Middle and Upper Permian. World-wide.Rem ark s: The Roadian Phaenicosphaera mammilla SHENG&WANG, 1985 has larger mammae.

Superfamily: RuzhencevispongaceaKOZUR,1980

S y non y m : Lalenlifislulacea NAZAROV& ORMISTON,1983

Family: LatentifistulidaeNAZAROV & ORMISTON, 1983

Genus: LatentifistulaNAZAROV & ORMISTON, 1983

Ty pes p e c i es: Lalenlifislula crux NAZAROV & ORMISTON,1983

Latentifistula n .sp.(PI. 2, Fig. 6)

Mat eri a I: 3 specimens.Description: 3 arms diverging at 120°. The arms be-come distalwards slightly wider. They are in the centralpart very high, terminally low. Pores small, irregularlyarranged. Inner features unknown.

Measurements:Length of arms = 235-241 J.Lm.Width of arms (central) = 64-71 J.Lm.Width of arms (subterminal, widest part) = 93-96 J.Lm.

Dis tri but ion: Dzhulfian of the Torrente San Calogerosection.

Rem ark s: This species is clearly distinguished from allother Lalenlifislula species by the cross section of thearms (very high in the central part, low in the distalpart).Unfortunately, the preservation is too bad for establish-ing a new species.

Suborder, superfamily and family inc.Genus: Gustefana n.gen.Der i vat ion 0mi n is: Arbitrary combination.Typ e s p e ci es: Guslefana obliqueannulala n .gen.Dia g nos is: Test large, slender conical to cylindrical.Pore frames consisting of oblique rings and often indis-tinct vertical ridges.

Assigned species:Guslefana obliqueannulala n.gen. n.sp.Guslefana sp.

Dis tri but ion: Abundant in the Upper Permian of West-ern Sicily.

Rem ark s: This genus is perhaps an aberrant represen-tative of the Ruzhencevispongacea KOZUR, 1980 withonly one arm. The internal structure is, however, un-known. Therefore the systematic position of the newgenus is uncertain.

Gustefana obliqueannulata n.gen. n.sp.(PI. 2, Figs. 8-10; PI. 3, Figs. 1,2,4, (?)6, 7, 8)

Derivatio nominis: According to the oblique porerings.

Holotype: The specimen on PI. 3, Fig. 1, rep.-no. CK1188/V1-38 M at e ria I: Several1000 specimens.

Dia g nos is: Large, slender, slightly conical test. Poreframes consisting of oblique rings and often indistinctvertical ridges.

Measurements:Length of test = 618-1065 J.Lm.Maximum width of test = 176-225 J.Lm.Minimum width oftest = 75-106 J.Lm.

Dis tri but ion: Abundant in the Dzhulfian of WesternSicily.

Rem ark s: Guslefana n.sp. has a cylindrical test.None ofthe numerous specimens is fully preserved. Theapical tip is always broken away. Despite ofthis fact, theform is described here, because it is one of the mostcharacteristic and abundant radiolarians of the Dzhul-fian in Western Sicily, and well distinguished from all hi-therto known radiolarians.

Gen. et spec. indet.(PI. 2, Fig. 4)

Material: 1 specimen.Rem ark s: This form with a globular shell and two roundpolar spines is probably a representative of the Entac-tinaria. The preservation is very bad and the inner struc-ture is unknown. Therefore the systematic position ofthis form is doubtful.

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Table1.Radiolarian zonation of the Tethyan and Circum-Pacific Permian.

Stage Substage Radiolarian Zone

Changxingian Neoa Ibai lIella grypa Zone

Neoal bai lIella ornithoformis ZoneDzhulfian Follicucullus ventricosus Ishigaconus-

scholasticus A.Z.--:::-------------charveti--- -- - Follicücull us - F. porrectus A.Z.-- -

Capitanian Follic.ucullus moriacanthus Zone

Parafollicucullus fusiformis -Wordian 'Parafol1icUcurtus globosus A. Z'~

Parafollicucullus longtanens is Zone

Roadian Spinodeflandrella foremanae -ParafollicucuHus corneJli A.Z.

Pseudoalbaillella rhombothoracata ZoneLeonardian

ParafolJicucullus ornatus Zone------------------Baigend zhi nian Parafollicucullus lomentarius A.Z.

ArtinskianAktastinian

SterlitamakianSakmarian

Tastubian Pseudoal baillella (Kitoconus) elegans Zone-----------------------------------------------------------------------------------Asselian Curvarbai lJella uforma A.Z.

Upper Gzhelian (Carbon iferoLAs) Curvalbai Ilelra bulbosa. Zone

4. Paleoecologic Evaluationof the Radiolarian Faunas

According to KOZUR(1991 a, b) the paleopsychrosphericostracod fauna from the radiolarian-bearing sample 655indicates psychrospheric conditions on the margin of theoceanic Permian Tethys. These conditions require an un-restricted deep-water connection to the world ocean toinclude these areas in the oceanic deep-water circulation.In subtropical to tropical areas to which belong the west-ernmost Tethys during the Permian, psychrospheric con-ditions indicate a water depth below 500 m.This paleoecologic evaluation of the ostracod faunas is

supported by other faunal elements. The conodonts con-sist of pelagic deep-water species of Circum-Pacificcharacter. Rich trace fossil associations in the Lower Per-mian part of the sequence belong to the deep-bathyal toabyssal Nereites ichnofacies with abundant Palaeodictyon.Also the radiolarian faunas with dominating Albaillella-

cea indicate unrestricted deep-water connections. Thiscould be confirmed by investigations of the Permian ra-diolarian faunas of the Delaware Basin. The Permian reefslope of the Guadalupe Mountains at the margin of theDelaware Basin corresponds to the present day SE slopeof the Guadalupe Mountains. The water depth during thedeposition of thePermian sequencein the Delaware Ba-sin is therefore wellknown.The shallow-wa-

ter radiolarian asso-ciation down to50 m water depthconsists almost ex-clusively of Copi-cyntrinae KOZUR&MOSTLER,1989. Theinterval of 50-500 mwater depth is domi-nated by Entacti-naria, accompaniedin the shallower wa-ter depths by Copi-cyntrinae, below200 m by the firstrare Albaillellacea.In water depth be-

low 500 m, Albaillel-lacea are domina-ting, accompaniedby variable amountsof Entactinaria,Ruzhencevisponga-cea and Phaenico-sphaera. With grow-ing distance fromthe margin of thebasin, the percen-tage of Entactinariadrops, whereas thepercentage of Al-baillellacea andpartly also of Phae-nicosphera in-creases.

Both the Lower Permian and the Dzhulfian radiolarianfaunas of Western Sicily are dominated by Albaillellaceaand Phaenicosphaera. Ruzhencevispongacea are rare. En-tactinaria are nearly missing. Copicyntrinae are missing.These radiolarian faunas indicate off-shore deep-waterassemblages. Similar assemblages are known from Per-mian cherts of Oman, China, Philippines and Japan.

5. Biostratigraphic Evaluationof the Radiolarian Faunas

Conodonts and radiolarians are the stratigraphicallymost important fossils in pelagic Permian deposits. Am-monoids are important as well, but in off-shore deep-wa-ter deposits, like in the Sicanian Paleogeographic Domainof Western Sicily, nearly absent. Only in the reef-slope orbase-of-slope deposits of the Sosio Limestone blocksand in olistoliths of facially similar rocks ammonoids havebeen found.In cherts and deep-water claystones and siltstones even

pelagic conodonts are very rare or absent and mostly re-presented by smooth gondolellids that are of lesser strati-graphic value than the often sculptured conodonts of

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near-shore or shallow pelagic environments. In these off-shore deep-water deposits the radiolarians are the strati-graphically most important fossils. The correlations ofthese radiolarian faunas with other faunas are, however,often difficult. Fusulinids and most of the conodont fau-nas, reported from such deposits, have been derived fromolistoliths or tectonic blocks inside these deep-water se-quences. These rocks have often a different age as theradiolarian-bearing matrix that is in general free of macro-fauna and barren or very poor in conodonts.

For the above reasons, the radiolarian successions areoften well known (Tab. 1), but their correlation with themarine Permian standard is still disputed. Radiolarian fau-nas of well dated Permian sequences, as in the DelawareBasin of West Texas and in the Sicanian PalaeogeographicDomain of Western Sicily, are therefore very important forthe correlation of the radiolarian zonation with the interna-tional standard.

Unfortunately, these radiolarian faunas have been erron-eously dated for long time. The red Dzhulfian claystones ofthe Sosio Valley have been placed for long time into theTertiary and only CATALANO,DI STEFANO& KOZUR(1988 a, b,1991, 1992) have proven an Upper Permian age for thesedeposits. Surprisingly, also the radiolarian faunas from theDelaware Basin have been erroneously dated (ORMISTON&BABCOCK, 1979; NAZAROV& ORMISTON, 1985; CORNELL &SIMPSON, 1985). Especially the dating of the Follicucullusventricosus-Ishigaconus scholasticus fauna of the uppermostLamar Limestone as Capitanian (Middle Permian) by OR-MISTON& BABCOCK(1979) and NAZAROV& ORMISTON(1985)has hindered very much the correct application of the ra-diolarian zonation in the Upper Permian of the Tethys.The F ventricosus-I. scholasticus radiolarian fauna was ori-

ginally described by ORMISTON& BABCOCK(1979) from theuppermost Lamar Limestone of a road cut on US Highway62-180. They placed this fauna in the Capitanian, likemost of the American authors before. Only FURNISH(1983)recognized that at least the larger part of the Lamar Lime-stone is post-Capitanian and he placed this member in hispost-Capitanian / pre-Dzhulfian Amarassian Stage.Re-investigations of the type locality of F ventricosus and

/. scholasticus (road cut on the US Highway 62-180) and ofother localities of the uppermost Lamar Limestone Mem-ber have shown that the F ventricosus-I. scholasticus fauna isaccompanied by Dzhulfian conodonts. In the underlyingbeds Mesogondolella "babcockae" (CLARK & BEHNKEN) is pre-sent. The holotype of this species is inseparable from M.postserrata BEHNKEN and therefore M. babcockae is a juniorsynonym of M. postserrata. However, most of the specimensplaced by CLARK & BEHNKEN(1979) into "Neogondolella" bab-cockae are separable from M. postserrata as an independentspecies.

In the lower Lamar Limestone typical M. postserrata, theCapitanian guideform, is present and M. "babcockae" (Meso-gondolella n.sp. A) is still absent. In these beds Yabeina la-marensis, an advanced Middle Permian (Capitanian) fusuli-nid is present. This genus is characteristic for the Abade-hian Stage Ounior synonym: Midian Stage) of the EurasianTethys. Therefore the lower Lamar Limestone belongs un-doubtedly to the Middle Permian Guadalupian Series (Ca-pitanian Stage).An Early Dzhulfian age of the uppermost Lamar Lime-

stone is not only indicated by conodonts (Clarkina chang-xingensis italica n. subsp., Clarkina n.sp., Mesogondolella n.sp.A), but also by the F ventricosus-I. scholasticus radiolarianfauna.

This fauna occurs in Japan in undoubtedly Dzhulfiandeposits. Because of the assumed Capitanian age of thetype material of these species in West Texas, the Japaneseradiolarian workers placed the F ventricosus-/. scholasticusZone in the upper Capitanian-Lower Dzhulfian. However,no Capitanian faunal elements occur together with theseradiolarians in Japan.The oldest radiolarian fauna of Late Permian character

in Japan is characterized by Follicucullus porrectus RUDENKO(= Follicucullus sCholasticus, morphotype II sensu ISHIGA,1984), F? charveti CARIDROIT& DEWEVER, Ishigaconus bipartitus(CARIDROIT& DE WEVER), Pseudoalbaillella eurasiatica KOZUR,KRAHL & MOSTLERand Nazarovella gracilis DE WEVER& CARI-DROIT.Both F ventricosus and I. scholasticus are not yet pre-sent in this fauna. However, F porrectus, common in thisfauna, is the direct forerunner of /. scholasticus. Undoubted-ly, this F? charveti-F porrectus fauna is older than the F ventri-cosus-/. scholasticus fauna of the uppermost Lamar Lime-stone that follows in Japan immediately above the F?charveti-F porrectusfauna (ISHIGA, 1984).The age of the F ? charveti-F porrectus fauna of Japan has

been well dated by ISHIGA& MIYAMOTO(1986). They couldprove that the F ? charveti-F porrectus fauna corresponds tothe Lepidolina kumaensis Zone of the fusulinid zonation.However, the shallow-water fusulinids may be reworkedand older than the Dzhulfian pelagic faunas (radiolarians,ammonoids).The age of the Lepidolina kumaensis Zone has been dis-

puted. Most of the Japanese Permian stratigraphersplaced this zone into the Dzhulfian. KOTLJARet al. (1989)have shown that this zone is older than the type Dzhulfianof Transcaucasia and they placed therefore the L. kumaensisZone into the "Midian Stage" Ounior synonym of theAbadehian that is, in turn, a junior synonym of the Capita-nian). However, the "Midian" / Dzhulfian boundary ofTranscaucasia is characterized by a facies-controlled im-migration of Dzhulfian fossils (fusulinids, brachiopods,conodonts, ammonoids, often in this order) on a sinkingcarbonate platform. The uppermost "Midian" rocks areextremely shallow-water algal-foraminifer limestones, inwhich even fusulinids are missing. The overlying lower-most Dzhulfian rocks are shallow pelagic, followed by pe-lagic ammonoid- and conodont-rich limestones. The im-migration of the Dzhulfian ammonoid- and conodont fau-nas is not contemporaneous with the first appearance ofthese faunas. The typical Dzhulfian araxoceratids amongthe ammonoids are already present in the L. kumaensisZone. This Zone has therefore already a Dzhulfian fauna,but it is older than the type Dzhulfian of Transcaucasia.The base of the Dzhulfian has to be redefined outside

the Dzhulfian type area. Best suitable are sections inSouth China, where in some places the Wuchiapingian fol-lows without break above the Middle Permian Maokouanwithin pelagic or shallow-water rocks. In this case,however, the term Dzhulfian should be replaced by theterm Wuchiapingian.

If the Lepidolina kumaensis Zone were finally placed into theDzhulfian (or Wuchiapingian), the largest part of the LamarLimestone of West Texas (all beds above the horizon withYabeina lamarensis in the lower Lamar Limestone) would beplaced into the Dzhulfian (or Wuchiapingian).All faunas above the Lepidolina kumaensis Zone in Japan

are undisputed Upper Permian (Dzhulfian and Chang-xingian). Thus, the Dzhulfian age ofthe F ventricosus-/. schol-asticus fauna (that follows immediately above the F ? charve-ti-F porrectus fauna of the Lepidolina kumaensis Zone), is un-

113


Text-Fig.4.Simplified paleogeographic reconstruction of the Permian Tethys during the Middle Permian time.Based on new data about the Permian of Sicily, Crete, Oman and Fariman (eastern Iran) by KOZUR&KRAHL(1987), CATALANO,DI STEFANO& KOZUR(1988 a, b, 1989, 1991, 1992), KOZUR(1989, 1991 a, b), DEWEVER,BOURDILLON-DEGRISSAC& BECHENNEC(1988), KOZUR& MOSTLER(1989, 1991).A = deep-water areas, partly oceanic. B = shallow-water areas, partly hypersaline; in Transcaucasia,centrallran and western Turkey during the Upper Permian also pelagic. The shallow-water areas are notshown in their full extent. Only the assumed boundary between deep-water and shallow-water is in-dicated. C= Place of the Dzhulfian-Lower Changxingian predominantly hypersaline Zechstein Basin. D= Place of the later opening of the northern branch of the early Tethys: toward the west until thePontides during the Dzhulfian, until the Transylvanides (Eastern Carpathians) during the Upper Scy-thian and in the Meliata-Hallstatt sphenochasma during the upper Lower Anisian and Pelsonian.1 = Middle Permian shallow-water deposits, partly with pelagic influx in Tunisia. 2 = Permian deep-wa-ter deposits and subordinate reef-slope deposits in western Sicily (Sicanian domain). 3 = shallow-wa-ter Middle and Upper Permian deposits of the Lagonegro domain in southern Apennines and its pos-sible prolongation (4) in the Imerese domain of Sicily. 5 = "Clastic Trogkofel Beds" with partly pelagicLower and basal Middle Permian, overlain by shallow-water Middle and Upper Permian limestones. 6 =Phyllite Unit of Crete with pelagic Bashkirian to Lower Triassic deposits. 7 = Middle Permian pelagiclimestones in Kurdestan, northeastern Iraq. 8 = Middle to Upper Permian radiolarites in Oman.

o•••

A.B.[f]:.C .:.:.:.:.:.

....." -...,..,

.........::..\...~"'rl'.....- :................i

. ......... \,

.... .....

Formation of the Delaware Basin has even pre-Artinskiancharacter.

The reason for this opinion is not clear. The S. foremanae-Pcornelli fauna is a transitional fauna between Lower andMiddle Permian radiolarian complexes. In other faunas(e.g. ammonoids, conodonts) such faunas with Middleand Lower Permian elements are characteristic for theRoadian, the lower Stage of the Middle Permian Guadalu-pian Series. For this reason, KOZUR & MOSTLER(1989) re-jected the correlation of the Bone Spring- and Cutoff For-mation with the Artinskian and they pointed out that theradiolarian fauna of the upper "Bone Spring Formation" ofthe Delaware Basin is considerably younger than the typeArtinskian and can not be older than Upper Chihsian (=uppermost Leonardian). This lowermost assignment wasnot based on radiolarians, but on conodonts, because theuppermost Bone Spring Formation contains Mesogondo/ellaidahoensis (YOUNGQUIST,HAWLEY & MILLER), an index spe-cies for the Chihsian (= middle and upper Leonardian).

In two excursions in spring 1991 under guidance of Prof.D. LEMoNE, EI Paso, and Prof. B.F. GLENISTER, Iowa City,numerous samples have been taken from the classical"Bone Spring Limestone" outcrop from a road cut on thenorthwestern side of the U.S. Highway 62-180,3 km NE of

far assumed, but Early Dzhulfian in age. The F venlricosus-/.scho/asticus Zone of Japan is therefore not of Late Capita-nian age (assumed because ofthe Capitanian assignmentof this fauna in West Texas) and Early Dzhulfian age (datedby accompanying faunas in Japan), but exclusively of Ear-ly Dzhulfian age.

This newage determination of the F venlricosus-/. scho/as-licus Zone in its type locality is very important for the agedetermination of the Upper Permian radiolarian fauna ofWestern Sicily. /shigaconus scho/asticus (ORMISTON & BAB-COCK) and the genus Cariver n. gen. are common in thisfauna. Both are restricted in Japan to the Upper Permianand Dzhulfian respectively. Mostlerispongus sosioensis n.sp. isalso known from the Upper Permian of the Philippines,figured as Oclalormenlum sp. Upper Dzhulfian and Chang-xingian radiolarians, like /moloella exce/sa (ISHIGA, KITO & IM-OTO), I. levis (ISHIGA, KITa & IMOTO).Neoa/baillella ornilhoformisTAKEMURA& NAKASEKO,N. optima ISHIGA, KITa & IMOTO,andN. grypa ISHIGA, KITO & IMOTO are missing in these beds.Therefore the radiolarian faunas of the lower part of the redclaystones and of the uppermost light-gray claystones inthe Torrente San Calogero section indicate Early Dzhulfianage.

This Dzhulfian age for the lower part of the red claystones of the Torrente San Ca-logero section is confirmed by theconodont fauna with C/arkina chang-xingensis ila/ica KOZUR, C. sosioensisGULLO & KOZUR and Hindeodus ty-picalis (SWEET).Changxingian con-odonts are missing in these beds.They are present in the upper partof the red claystones, where C. sub-carinala (SWEET), C. changxingensischangxingensis (WANG & WANG), C.deflecla (WANG & WANG) are com-mon. No determinable radio-larians have been found in theseChangxingian beds.

Whereas the Lower Permian isrich in Albaillellacea-dominatedradiolarian faunas of latest Artin-skian and Lower Leonardian age,described by KOZUR in CATALANOet al. (1989). the Middle Permianof the Sosio Valley area yielded sofar only few and badly preservedradiolarians. Only Parafollicuculluscornelli KOZUR & MOSTLER, 1989and Pseudoa/baillella cf. sea/praiaHOLDSWORTH& JONES, 1980 couldbe determined. P cornelli is an in-dex form of the Spinodeflandrella fore-manae-Parafollicucullus cornelli A.Z.The age of this fauna has beendisputed.

CORNELL & SIMPSON (1985) andNAZAROV & ORMISTON (1985) ori-ginally described this fauna fromthe "Bone Spring Limestone" ofthe Delaware Basin. NAZAROV &ORMISTON (1985) correlated theBone Spring Formation and over-lying Cutoff Formation with the Ar-tinskian of the Cis-Urals andpointed out that the radiolarianfauna from the upper Bone Spring

114


its junction with Texas Highway 54, S of the GuadalupeMountains (for locality data see CORNELL& SIMPSON, 1985,Text-Fig. 1). This is the type locality for all guideforms ofthe S. foremanae-Pcornelli A.Z.

According to a pers. comm. of Dr. L.L. LAMBERT, IowaCity, these beds do not belong to the Bone Spring Forma-tion, but to the upper Cuttoff Formation. This is confirmedby a conodont fauna with Mesogondolella nankingensis CHING[Uunior synonym: M. serrata (CLARK & ETHINGTON)]and Neo-streptognathodus clinei BEHNKEN. This conodont fauna ind-icates Roadian age, like the ammonoids (SPINOSA, FURN-ISH & GLENISTER,1975). By this the view of KOZUR & MOST-LER(1989) is confirmed that the S. foremanae-P cornelli Zoneis considerably younger than the Artinskian.

According to the above data, the S. foremanae-P cornelliZone belongs to the Roadian Stage. The radiolarians ofthe matrix of the Olistostrome Unit indicate therefore thesame age as the conodonts with Mesogondolella phosphorien-sis (YOUNGQUIST,HAWLEY& MILLER) and Sweetognathus sub-symmetricuSWANG, RITTER& CLARK. The latter species is oneof the Roadian index species.

6. Paleogeographic Implications

The presence of a Circum-Pacific, Albaillellacea-domi-nated off-shore deep-water radiolarian fauna throughoutthe Permian (at least since the uppermost Artinskian) in-dicates a broad, open deep-water connection of the Sica-nian Paleogeographic domain of Sicily with the PermianPacific. This is also indicated by the presence of paleo-psychrospheric ostracods (KOZUR, 1991 a, b), pelagic

conodonts and trace fossils of the deep-bathyal to abyss-al Nereites ichnofacies with Palaeodictyon.

This stable connection throughout the Permian indi-cates that the Permian oceanic Tethys reached by farfurther towards the W as so far assumed. This PermianWestern Tethys was situated in the S, immediately north ofGondwana (Text-Fig. 4). The Cimmerian Tethys in the N,otten designated as "Paleotethys", extended in the Lowerand Middle Permian not further toward the W than easternIran (westernmost proven occurrence: Fariman, easternIran, KOZUR & MOSTLER and RUTTNER[in RUTTNER, 1991 D.During the Upper Permian, the ritting in the Cimmerian(northern) Tethys continued until western Turkey, duringthe uppermost Scythian until the Transylvanids (EasternCarpathians) and in the Middle Triassic until the EasternAlps (Meliata-Hallstatt sphenochasma of the Cimmerianocean; KOZUR, 1991 a,b).

AcknowledgementsThe investigations in Texas and partly in Sicily have been sponsored by

the Deutsche Forschungsgemeinschaft. Former investigations in West-ern Sicily have been supported and sponsored bya working group of theDip. di Geologia e Geodesia, Palermo University, under leadership ofProf. R. CATALANO.The SEM photos have been taken in the above depart-ment and in the Geologicallnstitute of the Northern Arizona University,Flagstaff, Arizona. My investigations on the Texas radiolarians have beencarried out in the Museum of Northern Arizona in Flagstaff, Arizona, andsupported by all staff members, especially by Dr. M. MORALES.The excur-sions in Western Sicily have been guided by Dr. P. 01 STEFANO,Palermo. 4weeks excellent excursions in Texas and New Mexico have been guidedby Prof. O. LEMONE,EI Paso, Prof. P.A. GLENISTER,Iowa City, Prof. M.K.NESTELL,Arlington, and Dr. W.C. CORNELL,EI Paso.

I thank all the above organisations and colleagues for their very impor-tant help.

115


[ Plate 1 ]

If not otherwise indicated, all figured specimens have been derived from sample 655 of the Dzhulfian (UpperPermian) lower part of predominantly red claystones of the upper Claystone Unit of the Torrente San Calogerosection, SW of the Pietra di Salomone, Sosio Valley area, Western Sicily (Italy).

Figs. 1- 3: Ishigaeonus seholastieus (ORMISTON & BABCOCK); x 170.Fig. 1: rep.-no. CK/III-68.Fig. 2: rep.-no. CK/III-70.Fig. 3: rep.-no. CK/III-70A.

Figs. 4- 6: Follieueullus dilatatus RUDENKO; x 170.Fig. 4: rep.-no. CK/III-74.Fig. 5: rep.-no. CK/III-72.Fig. 6: rep.-no. CK/III-83.

Figs. 7-11: Follieueullus porreetus RUDENKO; x 170.Fig. 7: rep.-no. CK/III-81.Fig. 8: rep.-no. CK/III-71.Fig. 9: rep.-no. CK/III-80.Fig. 10: rep.-no. CK/III-82.Fig. 11: rep.-no. CK/III-73.

Figs. 12-14: Laeisus siphuneulus n.gen. n.sp.j x 170.Fig. 12: holotype, rep.-no. CK 1188NI-33.Fig. 13: rep.-no. CK/III-35.Fig. 14: rep.-no. CK/III-52.

Figs. 15-17,19: Cariver dorsoeonvexus n.sp.Fig. 15: x 170, rep.-no. CK/III-39.Fig. 16: holotype; x 170, rep.-no. CK/III-64.Fig. 17: x 170, rep.-no CK/III-66.Fig. 19: x 320, rep.-no. CK/III-45.

Fig. 18: Laeisus n.sp.; x 170.Rep.-no. CK/III-12.

Fig. 20: Parafollieueullus eonvexus (RUDENKO & PANASENKO); x 170.Upper part of apical horn and distal part of test broken away.Rep.-no. CK/III-26.

Figs. 21,22: Pseudoalbaillella eurasiatiea KOZURj KRAHL & MOSTLERj X 170.Fig. 21: rep.-no. CK/III-15.Fig. 22: rep.-no. CK/III-50.

Fig. 23: Parafollieueullus monaeanthus (ISHIGA & IMOTO); x 170.Rep.-no. CK 1188NI-24.

116


f

117


Fig. 1:

Fig. 2:

Fig. 3:

Fig. 4:

Fig. 5:

Fig. 6:

Figs.7,11,12:

[ Plate 2 ]


Phaenicosphaera mammifera (NAZAROV & ORMISTON).x 170, rep.-no. CK/III-59.

Urocyrtis? sp.x 320, rep.-no. CK/III-44.

Hindeosphaera? n.sp.x 320, rep.-no. CK/III-24.

gen. et spec. indet.x 170, rep.-no. CK/III-62.

Mostlerispongus sosioensis n.gen. n.sp.Holotype, x 170, rep.-no. CK/III-65.

Latentifistufa n.sp.x 170, rep.-no. CK/III-32.

Bryozoa.Fig. 7: Two zooids still connected, x 80, sample S 6 (out of sequence), olistolith or block of light-gray biogenic

limestone, uppermost Leonardian, Pietra dei Saracini, Sosio Valley area, Western Sicily, rep.-no. CK/VI-16.

Figs. 11,12: Single zooids, morphologically similar to advanced Follicucullidae, but unrelated to them, x 170.Fig. 11: Rep.-no. CK/III-31.

Fig. 12: Sample S 12 D, Wordian reef-slope limestone, Rupe del Passo di Burgio, Sosio Valley area, WesternSicily; rep.-no. CK/IV-50.

Figs. 8-10: Gustefana obfiqueannufata n.gen.sp.Fig. 8: x 170, rep.-no. CK 1188/V1-39.Fig. 9: x 170, rep.-no. CK 1188/V1-40.Fig. 10: x 80, rep.-no. CK/III-60.

118


119


[ Plate 3 J


Figs. 1,2,4,(?)6,7,8: Gustefana obliqueannulata n.gen. n.sp.Fig. 1: Holotype, x 160, rep.-no. CK 1188/V1-38.Fig. 2: x 160, rep.-no. CK 1188/V1-29.Fig. 4: x 80, rep.-no. CK 1188/ VI-40 A.Fig. 6: x 80, rep.-no. CK 1188/V1-37.Fig. 7: x 80, rep.-no. CK/III-61.Fig. 8: x 80, rep.-no. CK 1188/V1-27.

Figs. 3,5: Gustefana n.sp ..Fig. 3: x 160, rep.-no. CK 1188/V1-3.Fig. 5: x 80, specimen lost.

Figs. 9,11: Ishigaconus scholasticus (ORMISTON& BABCOCK).Specimens with fully preserved dorsal free columella sample 216, Delaware Basin (West Texas), road cut on USHighway 62-180 (section H by ORMISTON& BABCOCK, type locality of F. bispinosus, F. ventricosus and I. scholasticus),uppermost Lamar Limestone, 10 cm below the top of the section (about 0.5-1 m below the top of the LamarLimestone in this area). Lower Dzhulfian.Fig. 9: lateral view, x 200, rep.-no. N 4060.Fig. 11: oblique dorsal view, x 100, rep.-no. N 4063.

Fig. 10: Follicucullus ventricosus ORMISTON& BABCOCK, lateral view.x 100, sample 216 (see Figs. 9, 11), rep.-no. N 4069.

Figs. 12,14: Follicucullus bispinosus n.sp ..Lateral views, x 100, sample 216 (see Figs. 9, 11).Fig. 12: rep.-no. N 4061.Fig. 14: holotype, rep.-no. 4062.

Fig. 13: Stigmosphaerostylus itsukaichiensis (ISHIGA& TONISHI).X 100, sample 216 (see Figs. 9, 11).

120


121


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Manuskript bei der Schriftleitung eingelangt am 30. April 1992

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