Precambrian? and Cambrian stratigraphy of the Penbegli-Tut ... · Precambrian? and Cambrian stratigraphy of the Penbegli-Tut inlier, ... structural divisions of Turkey and location

Geol.Mag. 134(7), 1997. pp. 37—53. Copyright© 1997 Cambridge University Press 37

Precambrian? and Cambrian stratigraphy of the Penbegli-Tut inlier, southeastern Turkey

W. T. DEAN*, F. M A R T IN I, O. M ONOD}, Y. GÜNAYlj, H. KOZLUH & N. BOZD OG AN|[

* Department of Earth Sciences, P.O. Box 914, University of Wales Cardiff, Cardiff CF1 3YE, UK I Département de Paléontologie, Institut royal des Sciences naturelles de Belgique, rue Vautier 29, B-1040 Brussels,

Belgium (deceased)} Laboratoire de Géologie Structurale, Université d’Orléans, B.P. 6759,45067 Orléans Cedex 2, France

T Turkish Petroleum Corporation, Ankara 06520, Turkey

(Received 4 May 1995; revised version received 7 August 1996; accepted 13 August 1996)

Abstract - The oldest rocks in the Penbegli-Tut inlier of southeastern Turkey belong to the Meryemu§agi Formation (base not seen); they are mostly clastic rocks of ?late Precambrian age, overlain with angular unconformity by unfossiliferous quartzites (270 mest.) oftheZabuk Formation. The latter unit is succeeded conformably by the Koruk Formation (Lower?/Middle Cambrian), comprising almost 200 m of dolomite and grey and red nodular limestone, and the Sosink Formation (Middle Cambrian), about 600 m of silty mudstone and sandstone with a few thin limestone beds, overlain unconfonnably by Cretaceous carbonates. The closest comparison is with the Derik-Mardin area, 220 km to the east, where the section is more complete. The upper Koruk Formation contains trilobites of the Pardailhania and Solenopleuropsis biozones; trilobites from the Sosink Formation indicate the Solenopleuropsis Biozone, a post -Solenopleuropsis interval, and a level with Holasaphus mesopotamicus, known only from the Derik area. Acritarchs from the highest Koruk Formation and the whole of the Sosink belong to the lower part of microflora A2, described from tile Middle Cambrian of eastern Newfoundland.

1. Introduction

Lower Palaeozoic outcrops in the Penbegli-Tut area, about 75 km east-northeast of Kahra manina raç. form one of a group of inliers of various sizes that are distributed along the Arabian Platform in southeastern Turkey. Apart from the Derik-Mardin area, which belongs to the stable foreland, most of the Palaeozoic outcrops, such as the Hazro anticline and the Great Zap anticline, south of Hakkâri (Fig. 1), are situated in the Border Folds zone of Ketin ( 1966«). In the northern Border Folds, other Palaeozoic outcrops appear from beneath large ophiolitic nappes, either within small tectonic windows, such as at Penbegli-Tut and in the Korudag anticline along the River Euphrates, 120 km to the east-northeast (Perinçek, 1979), or in much larger areas such as the central and southern Amanos Mountains (Yalçin, 1980; Dean, Monod& Gtinay, 1986;Yilmaz, 1993).

The Lower Palaeozoic succession in the Penbegli-Tut inlier is essentially of Cambrian age. The area is of particular interest as it forms a link between the Cambrian rocks of the Taurides and Amanos Mountains to the west, and those of the Derik-Mardin inliers and the Hakkâri region further southeast in Turkey (Fig. 1). The present account reviews briefly the principal lithologies and unit boundaries, their ages, and their relationships with corresponding strata elsewhere in southern Turkey.

Relatively little lias been published on the area. The first account was by Ketin (19666), who produced a general cross-section and divided the succession as follows: Mcrvcmusagi Formation; C l or Kaplandere Formation;

C2 or Dolomite Formation; and C3 or Ycrlikas Formation, overlain with marked unconformity by transgressée upper Cretaceous rocks. C3 was held to be Middle Cambrian in age as it contained the trilobite Paradoxides; C l and C2 were placed tentatively in the Lower Cambrian, and the Mciycmusagi Formation in the ‘Infra- Cambrian’. Following a preliminary visit in 1968, Dean (1975, p. 364) noted the presence of pink and grey nodular limestones in the Ycrlikas Formation near Küçük Perveri, and confirmed the presence of Paradoxides (s. I.) and Solenopleuropsis together in the same unit.

More recently the area was systematically mapped under the direction of the late Ozan Sungurlu as part of an unpublished report for Turkish Petroleum Corporation (T.P.A.O.), who have kindly permitted us to to publish the results both of this mapping (Fig. 2) and of fieldwork by the present authors in 1991 and 1992. We use here (Fig. 4) the litho stratigraphie terms now recognized by T.P.A.O., in ascending order as follows, with Ketin’s units in parentheses: Mciy cmusagi Formation; Zabuk Formation (Cl); Koruk Formation (C2); and Sosink Formation (C3). Only the Sosink Formation and the upper part of the Koruk Formation yielded trilobites and/or acritarchs, all of Middle Cambrian age. The former include representatives of four different faunas: (1) Pardailhania Biozone; (2) Solenopleuropsis Biozone; (3) post-Solenopleuropsis interval; and (4) Holasaphus mesopotamicus level. No Lower Cambrian macrofossils have been found in the inlier and the Middle Cambrian trilobites are mostly genera widespread in the Mediterranean region. In the Middle

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38 W. T. D E A N A N D OTHERS

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Cambrian of Spain Sdzuy (1968) recognized four trilobite-based stages, a sequence subsequently refined (Sdzuy, 1971) to include: a unit corresponding to the range of Paradoxides (Acadoparadoxides) mureroensis and Alanisia hastata; five successive ‘stages’ of Conocoryphe ovata, Acadolenus, Badulesia, Pardailhania and Solenopleuropsis; and finally, a ‘stage without Solenopleuropsidae’. Sdzuy (1972) retained the units and drew the Lower/Middle Cambrian boundary below the ‘Schichten mit P. mureroensis’, but the terms were formalized as zones by Palmer (1979) and used in a similar sense by Thomas, Owens & Rushton (1984), although both these publications omitted the ‘stage without Solenopleuropsidae’. For present purposes it has been found appropriate to employ the units as biozones. Sdzuy, Liñán & Perejon (1990), followed by Liñán, Perejon & Sdzuy (1993), proposed a number of Lower and Middle Cambrian stages based on the Spanish succession. Of the latter, only the Caesaraugustian Stage concerns us here as it comprises successive Badulesia, Pardailhania and Solenopleuropsis biozones, the two last of which are confirmed at Penbegli-Tut. The overlying so-called ‘Solenopleuropsidae-free Stage’ in Spain, used here as ‘post-Solenopleuropsis interval’, is represented in the inlier by most of the Sosink Formation, the highest beds of which include a Holasaphus mesopotamicus level not yet known outside southeastern Turkey. The terms early, middle and late Middle Cambrian used here correspond broadly to the ‘Stages’ of: A. Paradoxides oelandicus, B. Paradoxides paradoxiss imus, and C. Paradoxides forchhammeri, proposed for Scandinavia by Westergârd (1946). These units correspond to biozones in the Mediterranean region approximately as follows: (A) Acadoparadoxides mureroensis, Conocoryphe ovata, Acadolenus; (B) Badulesia, Pardailhania, Solenopleuropsis; and (C) post-Solenopleuropsis interval.

Unlike the trilobites, acritarchs obtained from the highest Koruk Formation to the top of the exposed Sosink Formation belong to a single assemblage, best compared with that in the lower part of Middle Cambrian microflora A2 in eastern Newfoundland (Martin & Dean, 1988), which ranges from highest Ptychagnostuspunctu- osus Biozone to, questionably, lowest Lejopyge laevigata Biozone. Because of the homogeneity of composition of the assemblage, the acritarchs are treated separately here to avoid repetition.

The Penbegli-Tut Palaeozoic inlier is situated near the Neogene triple junction of Kahramanmara? (sometimes Mara?) (Karig & Kozlu, 1990; Chorowicz et al. 1994), a few kilometres south and east of the active East Anatolian Fault (Fig. 2). The Palaeozoic outcrops extend discontin- uously more than 25 km along a conspicuous, east-west, left lateral oblique slip fault (Ini?dere Fault) which brings para-autochthonous Palaeozoic formations to the surface on its southern side against allochthonous units (Koçali ophiolite) and thick Tertiary cover on its northern side. On the upthrow side, the Ini?dere Fault is responsible for the unexpected, inverted position of the Palaeozoic rocks east of the Göksu valley, between the villages of Mery emu? agi and Tut. The elongated Palaeozoic outcrops thus appear as the core of a faulted, southerly reclined anticline. This structure also involves the Derdere Formation and Kastel Formation (carbonates and flysch, both of late Cretaceous age and undivided in Fig. 2), as well as the overlying Koçali ophiolitic unit. Further south (Körkün Dag) the ophiolitic rocks are directly overlain by Germav Formation (green marls, probably Palaeocene) and Miocene deposits, forming a syncline parallel to the Saytepe Fault. This suggests a late Tertiary to Recent age for the latest wrench tectonics, resulting from the ongoing collision of the Arabian Platform.

Two cross-sections are presented here (Figs 2, 3): one (E-F), south of Perveri, passes through stratigraphie

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sections A and B that have been measured and sampled near Devret village; the other (C-D) cuts through Kaplandere valley near the Yerlika§ locality described by Ketin (1966b). Both sections show the normal succession of Palaeozoic formations as well as the low-angle unconformity separating the Cambrian rocks from the Cenomanian Derdere Formation. Only to the east of Tut do Cretaceous carbonates rest directly on the Meryemu§agi Formation, as they do on the Telbesmi Formation at the classic section near Derik.

Although the area is generally referred to as the Penbegli-Tut inlier, recent editions of the topographic map show minor changes of place-names compared with those in the original accounts. Penbegli is now Akçabel, Perveri is Harmanli, and Küçük Perveri (or Küçükperveri) is replaced by Kalemta§; but for convenience both old and new names are shown on the present geological map.

2. Precambrian? and Cambrian stratigraphy

2.a. Meryemu^agi Formation

2. a. 1. Lithostratigraphy and possible age

The name was proposed by Ketin (1966Z?, p. 81) for a heterogeneous sequence of unfossiliferous clastic sediments that crops out both east of the River Göksu (= Göksu Çay), at and east of Meryemu§agi village, and west of it, in the lower part of Kaplandere valley. As first described the succession comprises, in ascending order: dark shale, glauconitic sandstone and greywacke, dark-green siltstone and shale, and dark-red sandstone and shale, with a 10 m diabase sill at the top. The top of the formation is

not exposed, and the thickness estimated by Ketin (1966Z?, p. 81, pi. I) was more than 300 m. No ductile deformation is present in the formation.

No macrofossils were recorded in outcrops at and south of Meryemu§agi, and no acritarchs were identified in the highest beds at the section along the road 1.8 km east of the village, and east of its junction with the road to Çanakci (Fig. 2; samples TUT-12 to 15). Organic material, although abundant, was not determinable; no firm age assessment is proposed, but it is probably no older than late Precambrian. A questionably similar age is supported by the stratigraphie relationships.

2.a.2. Correlation with other areas in southern Turkey

From its stratigraphie position the Meryemu§agi Formation was considered by Ketin to be of ‘Infra- cambrian’ or 4Eo-Cambrian = early Cambrian’ age, corresponding to volcanic rocks, 2400 m thick, of the Telbismi (= Telbesmi) Formation (Ketin, 1966Z?) or Derik Formation (Schmidt, 1965) in the Derik-Mardin area, 220 km to the east. More recently Wolfart (1983, p. 15 & Correlation Chart) listed Meryemu§agi Formation as a junior synonym of Çamlipinar Formation (Ketin, 1966b, p. 83), based on a type area in the Amanos Mountains; quite apart from possible lithological differences, the former name has page priority and is retained here. The position of the Meryemu§agi Formation immediately below unconformable quartzites of the Zabuk Formation at Kaplandere suggests that it may correspond in part to the Telbesmi Formation of Kellogg (1960), of uncertain age, but there is no lithological comparison between the two.

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Precambrian? and Cambrian stratigraphy, Southeastern Turkey 41

2. b. Zabuk Formation

2.b.l. Lithostratigraphy and possible age

The term was introduced by Schmidt (1965) in a stratigraphie chart which, although not formally published, was both widely circulated by the Turkish Association of Petroleum Geologists and in general use by the petroleum industry. The name was founded in the Derik-Mardin area for a quartzite-sandstone unit, underlain by red beds of the Sadan Fonnation (late Precambrian?) and overlain by limestones and dolomites of the Koruk Fonnation (Cambrian). The Zabuk Fonnation conesponds to Ketin’s ( 1966/r p. 81) Kaplandere Fonnation, described as 115-175 m of often red or purple siliciclastics, including conglomerates, sandstones, both cross-bedded and thinly- bedded, with a ‘diabase layer’ (?sill), 25 m thick, at the top. At the section near the east end of Kaplandere valley the unit has an estimated thickness of 270 m and overlies the Mciy cmusagi Fonnation with angular unconfonnity.

2.b.2. Correlation with other areas in southern Turkey

The fonnation was supposed by Sclnnidt to be of Cambrian age in the Derik area, but no evidence of fossils has been found there or at Kaplandere, and the questionable Lower Cambrian age shown in Figure 4 reflects the apparently confonnable relationship with the Koruk Fonnation. On purely lithological grounds the Zabuk Fonnation could possibly be conelated with the Htidai Quartzite Fonnation (Özgül in Dean & Özgül, 1994) of the western Taurides, which underlies fossiliferous basal Middle Cambrian carbonates and may therefore be of late Lower Cambrian age.

2.C. Koruk Formation

2.C.I. Lithostratigraphy

The fonnation name was introduced by Sclnnidt (1965) for a limestone/dolomite unit of unstated thickness with type section in the Derik area, 220 km east-southeast of the Göksu valley. Ketin’s (19666) later usage at Derik of ‘Sosink or Koruk fonnation’ is equivalent to what we interpret here as Sosink Fonnation together with the nodular limestones in the highest part of the Koruk Fonnation.

In the Penbegli-Tut inlier carbonate rocks between the quartzites of the Zabuk Fonnation and the predominantly siltstone/shale succession of the Sosink Fonnation fonn a compact, easily recognized unit, almost 200 m thick. On the south side of the Kaplandere valley (Figs 4, 5) about 170 m of thickly- and medium-bedded, grey, coarsegrained dolomite with stromatolites are followed by up to 23 m of grey and red nodular limestone and red shale. The unit conesponds broadly to the ‘Dolomite Fonnation’ of Ketin (19666, p. 83) whose description, however, made no mention of the red and grey nodular limestones. Interbeds of red silty mudstone occur especially in the highest 5.7 m, which are followed by

brown-weathering, grey silty shales of the basal Sosink Fonnation.

The ‘Küçükperveri’ area, about 5 km west of the Kaplandere valley, although established in the published literature, refers to a village whose name was recently changed to Kalcmtas. It is situated 2 km north-northeast of the two sections here recorded, which are best reached by a track leading south from a new, small village named Devret (Fig. 2). The sections, 1 km south of the latter, are here tenned Devret A (the more northerly) and Devret B. Although immediately adjacent to one another, they are separated by a nonnal fault with estimated throw of about 30 m, and differ only in detail from each other and from the Kaplandere section. At Devret A, no reliable thickness could be measured for the tliickly-bedded dolomites, but they are succeeded in turn by 8.5 m of red nodular limestone facies, and a 4.2 m unit of grey, nodular limestone and siltstone which is followed by yellow-brown weathering silty shales and siltstones typical of the Sosink Fonnation. At Devret B, the generally dolomitic succession above the faulted base comprises about 37 m of alternating lithologies that range from thickly-bedded, coarse- to fine-grained dolomite, through black micrite and grey calcarenite to calcareous breccia. The highest 14.5 m ofthe Koruk Fonnation begin with 6 m of nodular limestone and calcareous siltstone, pass through 7 m of shales with tliinly-bedded siltstone and nodular siltstone, and end with a resistant 1.5 m bed of siltstone and silty limestone below continuous silty shales of typical Sosink type.

2. c. 2. Biostratigraphv: macrofossils

Grey and red nodular limestones and shales fonning the upper part of the Koruk Fonnation are the oldest rocks in the Penbegli-Tut inlier to be dated with reasonable confidence. No fossils of any sort were found in the dolomite succession at the Kaplandere section, but trilobite fragments were collected sporadically through some of the overlying white sparitic and calcarenitic beds intercalated in the red nodular, micritic limestones, from which macrofossils proved difficult or impossible to extract. Genera include keronopsis, Eccaparadoxides, Conocoryphe and Dorvpyge, all of which have an extended range within the Middle Cambrian. The soleno- pleurid genus Pardailhania was found rarely in approximately the median 10 m of the 23 m unit (Figs 4, 5; Iocs FOB-74, OFB-44), which are assigned to the Pardailhania Biozone.

The highest 6.4 m of the Koruk Fonnation at the Kaplandere section yielded no macrofossils and, with the lowest 10 m of the Sosink Fonnation, constitute an interval of uncertain zonal position below the lowest record (Fig. 4, sample FOB-72) in this area of the succeeding biozonal trilobite genus Solenopleuropsis.

At neither Devret A nor Devret B (Fig. 6) did the Koruk Fonnation prove as fossiliferous as at Kaplandere, and Pardailhania was not recorded. Trilobites were rare

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but at Devret A, which is less well exposed and less complete than Devret B, Solenopleuropsis sp. was collected both from the highest few centimetres (sample FOB-80) of the Koruk Fonnation and at a level (sample OFB-50)4.4 m above the base of the overlying Sosink Fonnation. The same biozonal genus was found (sample OFB-51)1.4 m below the top of the Koruk Fonnation at Devret B, but the lower part of the unit there yielded only Conocoryphe (s.l.) sp. (samples FOB-81, 82) and Derikaspis sp. (sample FOB-83), neither of which is of zonal value.

2. c. 3. Correlation with other areas in southern Turkey

The bedded dolomites and nodular limestones of the Koruk Fonnation in the Penbegli-Tut inlier invite comparison with the Çal Tepe Fonnation of the western Taurids (Dean & Monod, 1970), and the two units are certainly contemporaneous in part. At the Çal Tepe stratotype, the fonnation is divided into four members, in ascending order: Dolomite (base unexposed). Black Limestone, Light-grey Limestone, and Red Nodular Limestone. However, near Hadim the Dolomite Member is underlain by a dark shale unit (Özgül in Özgül & Gedik, 1973); conesponding strata in the SultanDagarea were tenned Ardicli-Tepe-Schichten by Haude (1972, p. 413) and later ranked as a fonnation by Wolfart (1983, p. 14). The Black Limestone and Light-grey Limestone members are not developed at Penbegli-Tut. The type section of the Koruk Fonnation near Derik has still to be revised in detail, and for the present we retain the two fonnational names.

In the southern part of the Amanos Dag, 200 km southwest of Penbegli-Tut, Badulesia, index genus for the lowest trilobite biozone of the middle Middle Cambrian, occurs in mudstones of the lowest Sosink Fonnation (Dean, Monod & Günay, 1986), and the red nodular limestones of the highest Koruk are older than those at Kaplandere. Solenopleuropsis was recorded from higher in the Sosink Fonnation of the southern Amanos {loc. cit. ), but Pardailhania lias not yet been found there.

The oldest, dated occunence of the red nodular limestone facies so far documented is in the westernmost Taurides (Dean et al. 1993; Dean & Özgül, 1994) where, in the highest Çal Tepe Fonnation near Hüdai, southwest of Afyon (Fig. 1), it contains Acadoparadoxides (Acadoparadoxides) mureroensis (Sdzuy, 1958), index trilobite of the earliest Middle Cambrian biozone in Spain (Sdzuy, 1971). In the Çal Tepe-Hadim area of the western Taurides. Icado. (Acado.) mureroensis occurs about 10 m below the onset of the red nodular limestones facies. The higher red nodular limestones there and the lowest few metres of succeeding elastics, the Scydischir Fonnation, both contain Pardailhania (Dean & Özgül, 1981). Badulesia and Solenopleuropsis are unknown from Çal Tepe-Hadim, but in the Sultan Dag area Shergold & Sdzuy (1984) documented a Pardailhania fauna and a Solenopleuropsis fauna from the essentially clastic strata

of the Scydischir Fonnation. The red nodular limestone facies is clearly diachronous within the Taurides, as well as in the southern Amanos and Border Folds (Fig. 7). In general the facies becomes younger from west to east, and its age in the structurally discrete Amanos region is anomalous. The occunence of Badulesia there is so far unique in Turkey, and rocks of probably similar age in other parts of the country have proved unfossiliferous.

2.d. Sosink Formation

2.d.l. Lithostratigraphy

The tenn was used first by Kellogg (1960) for a mainly siltstone-sandstone succession, 1057 m thick, in the Sosink area, near Derik, 220 km east of Tut. Some of the lithologies in the Penbegli-Tut inlier closely resemble those of the type section, but the lowest 225 m at Sosink comprise grey mudstone with thin beds of limestone which yielded trilobites indicating both the Solenopleuropsis Biozone and still higher levels in the Middle Cambrian (Dean, 1982, pp. 35-7); corresponding lithologies and faunas are poorly represented at Kaplandere and Devret. We consider the Ycrlikas Fonnation of Ketin (1966A p. 83), named for a section 2.5 km east of Penbegli (Fig. 2), to be a synonym of Sosink Fonnation. According to Ketin the thickness is 70 m in the western part of the inlier and increases to 270 m in the east, but this is probably due to overstep at the base of the unconfonnable Cretaceous rocks.

2.d.l.a. Kaplandere area

The confonnable boundary between the Koruk and Sosink fonnations is visible at the west end of Kaplandere. Succeeding, retrogressively weathering strata assigned to the Sosink Fonnation consist mostly of grey, silty mudstone, weathering light-brown, with occasional thin (5 cm) beds of grey siltstone or limestone. In this section the unit has an estimated thickness of about 600 m, much of which is poorly exposed. The highest strata immediately below the Cretaceous unconfonnity are fissile mudstones which yielded several examples of the trilobite Holasaphus mesopotamicus Dean (1972) beside the track from Penbegli to Küçükperveri (Fig. 2, sample FOB-71).

2.d.l.b. Küçükperveri ’area

The lowest 9.5 m of the Sosink Fonnation are exposed in the east side of the valley at Devret A (Figs 2, 3, 6), the more northerly of the two sections. The top of the sequence is faulted against Koruk Fonnation, so that the lower part of the Sosink Fonnation is repeated about 50 m to the south, at Devret B section, where a succession some 240 m thick is exposed. Most of the lower strata comprise brown-weathering, grey, silty mudstone with rare, thin (5 cm) beds of limestone and calcarenite, but there is a progressive increase upwards in the development of

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SYSTEM AMANOS PENBEGLÍ DERÍK - ZAP& SERIES MOUNTAINS -TUT MARDIN VALLEY

Devonian(O.R.S.facies)

LL

T remadoc

~0

LL

LL

?Zabuk Fm.’Zabuk Fm Zabuk FmZabuk Fm

? PRE - CAM BR IAN Telbesmi Fm.

(Derik Voles.)'Sacian Fm. __ . Meryem- -

_ usagi Fm. • (no outcrop)

Figure 7. Table showing correlation of Cambrian rocks in the Amanos Mountains and Border Folds, and diachronism of the red nodular limestone facies in the region.

JQURNAL8 I



sandstone, both medium- and tliickly-bedded. About 208 m above the base of the fonnation there is a marked change to an incompletely exposed sequence of quartzites, the lowest 3 m cross-bedded, which persists up to and beyond the top of the hill, where the unconfonnable contact with overlying Cretaceous rocks is situated.

2.d.2. Biostratigraphv: macrofossils

2.d.2.a. Kaplandere area

Very few macrofossils were found, but a 5 cm limestone bed 10 m above the fonnation base (Fig. 5, sample FOB- 72) yielded trilobite debris, including Eccaparadoxidesl sp. and the biozonal index Solenopleuropsis sp. Material from 81m higher in the main section was confined to fragments of Eccaparadoxides sp. (Fig. 4, sample FOB- 77), indicating only an undivided Middle Cambrian age.

Holasaphus mesopotamicus in the highest beds was described from the middle of the type Sosink Fonnation, southeast of Derik, about 450 m (estimated) above its base. The species is not yet known outside southeastern Turkey, and its age has been put at Middle, possibly latest Middle, Cambrian (Dean, 1982, p. 37), but the trilobite evidence is not conclusive and no associated paradoxi- dids have been found either at Sosink or at Kaplandere.

2. d. 2. b. Küçükperveri ’area

At Devret A section decalcified muddy siltstone (sample OFB-50) 4.5 m above the base of the Sosink Fonnation yielded numerous fragments of Eccaparadoxides sp. and Solenopleuropsis sp. Thin beds of limestone were found rarely at Devret B, with macrofossils at only two levels (samples OBF-50/51, OBF-53; Fig. 6), respectively 107 m and 182 m above the fonnation base. The fonner level contained Solenopleuropsis sp., Derikaspis sp. and Eccaparadoxides sp., an assemblage indicative of the Solenopleuropsis Biozone and having much in coimnon with the lowest part of the type Sosink Fonnation. OBF- 53 yielded Derikaspis sp. m á Acadoparadoxides pentagonalis (Dean, 1982, p. 21), a species described from deposits at Sosink considered to post-date the Solenopleuropsis Biozone. In the Montagne Noire, southern France, probably equivalent strata, tenned Niveau I by Courtessole (1973), also contain, inter alia, Derikaspis (Dean, 1982; Courtessole, Pillet & Vizcaino, 1988). No trace of the Holasaphus mesopotamicus fauna was found under the Cambrian/Cretaceous contact in the vicinity of Devret B.

2.d.3. Correlation with other areas in southern Turkey

Close links with at least the lower half of the type Sosink Fonnation are evident, and both units contain Solenopleuropsis near the base. Fossiliferous, thin carbonate horizons are much more common in the lowest 225 m at the Sosink section, where the trilobite fauna is varied, relatively abundant (Dean, 1982), and cone

sponds in age to at least part of Sdzuy’s (1971) ‘Piso sin Solenopleuropsidae’ (late Middle Cambrian). The age of the Holasaphus mesopotamicus fauna is not precisely known in tenns of trilobite biozones, but the postulated late Middle Cambrian age receives support from the acritarchs. The upper half of the type Sosink Fonnation has not been sampled in detail and could be of late Middle to Late Cambrian age.

The lowest Sosink Fonnation in the southern Amanos Mountains (Dean, Monod & Gfinay, 1986) contains the biozonal trilobite Badulesia and is notably older than at Sosink or Penbegli-Tut. Solenopleuropsis occurs in the higher Sosink of the Amanos, but no evidence of the intervening Pardailhania Biozone lias been found there. In the Sultan Dag area, western Taurides, Shergold & Sdzuy (1984) demonstrated the presence in the Scydischir Fonnation of what they tenned ‘the Solenopleuropsis Fauna’, but the genus lias not yet been found in intervening parts of southern Turkey.

3. Notes on acritarchs

The oldest strata in the inlier to yield acritarchs are the highest transitional beds at the top of the Koruk Fonnation, and the lowest part of the Sosink Fonnation, primarily at Kaplandere (Fig. 5) and secondarily at Devret A (Fig. 6). The level is slightly below the top of the middle Middle Cambrian, in deposits which lack trilobites but lie between the Pardailhania and Solenopleuropsis biozones. Younger acritarch-bearing beds fonn part of the Sosink Fonnation and range in age from the highest part of the middle Middle Cambrian {Solenopleuropsis Biozone) through an undated portion of the post-Solenopleuropsis interval, which is either latest middle or early late Middle Cambrian. The remainder of the section is incompletely investigated and the youngest specimens from the Sosink Fonnation at Kaplandere were from samples (Fig. 4) 2 m below (TUT- 30) and 2 m above (TUT-3) the Holasaphus mesopotamicus level, which is postulated as approximately latest Middle Cambrian in age. The highest deposits of the Sosink Fonnation at Devret B (Fig. 6) are also incompletely exposed below the Cretaceous basal unconformity; KUC-23 and KUC-24 are from levels 307 m and 237 m (estimated) above the fonnation base, and belong to the post-Solenopleuropsis interval.

Acritarchs are abundant and well preserved in most samples. With few exceptions the same taxa are present, but in variable abundance, from the oldest levels (highest Koruk Fonnation) to the youngest (Sosink Fonnation), the ages of which cannot be separated on the basis of acritarchs, although the trilobites indicate four different horizons within the Middle Cambrian.

The assemblage always includes, generally in abundance, Timofeevia ¡ancorae (Cramer & Diez) Vangues- taine, 1978 (Fig. 9f, g, m-o) with relatively short processes like those described by Albani, Massa & Tongiorgi (1991), T. phosphoritica Vanguestaine, 1978

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48 W. T. D E A N A N D O THERS

Figure 8. For legend, see lacing page.

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(Fig. 9c, i) and, especially, fonns transitional (Fig. 9h, j—1) between these two species. Ann ul um squamaceum (Volková) Martin in Martin & Dean, 1983 (Fig. 8o) is found very frequently, although in small numbers. Cristallinium cambriense (Slavikova) Vanguestaine, 1978 (Fig. 8s, t), the generic assigmnent of which was confirmed by Martin in Young et al. (1994, p. 355), Eliasum Ilani scum Fombella, 1977 (Fig. 8i, j). Micrhystridium lanceolatum Vanguestaine, 1974 (Fig. 8h, 1-n, q, r, u, x). Multiplicisphaeridium martae Cramer & Diez, 1972 (Fig. 8a-e), Timofeevia manota Albani, Massa & Tongiorgi, 1991 (Fig. 9a, b, d, e), coenobial acritarchs sensu Di Milia, 1991 (Fig. 8v, w), and ubiquitous taxa such as sphaeromorphs, including Dichotisphaera sp. (Fig. 8g), are present in most samples, where they vary from rare to very numerous.

On the other hand Cristallinium ovíllense (Cramer & Diez) Martin in Martin & Dean, 1981 (Fig. 8p) and Comasphaeridium longispinosum Hagenfeldt, 1989 (Fig. 8k) are found only very occasionally in strata without trilobites which are situated above the Pardailhania Biozone and range higher, including the Solenopleuropsis Biozone. The fonner species was identified at KUC-32, KUC-6 and TUT-6, and the latter at TUT-23 and KUC-2. A single example of Pirea? sp. (Fig. 8f) was found at TUT-11, in a succession without zonal trilobites but about 78 m above FOB-72, with Solenopleuropsis sp.; the level (Fig. 5) is 2 m below FOB-77, which contains only Eccaparadoxides sp.

Comparison is best made with the trilobite-controlled acritarch zonation proposed for eastern Newfoundland (Martin & Dean, 1981, 1988). The presence of Cristallinium cambriense, Timofee\’ia 1ancorae and T. phosphoritica, with or without Eliasum Ilani scum, and the clear absence of Timofeevia pentagonalis and Vulcanisphaera turbata indicate that these acritarchs, from the Penbegli-Tut inlier and on the margin of the Arabian Platform, belong to the lower part of microflora A2. Similar coimnents apply to samples from imprecisely located levels within the Sosink Fonnation of the Derik- Mardin area, southeastern Turkey (Erkmen & Bozdogan, 1981). The lower part of microflora A2 at Manuels River and Random Island, eastern Newfoundland, corresponds to a fairly poorly-preserved assemblage which contains

only the four above species. It comes from an interval that ranges from late middle Middle Cambrian (‘Paradoxides davidis Zone’) to late late Middle Cambrian, at a level conelated with the Paradoxides forchhammeri ‘Stage’ and beneath the upper part of the (questionably developed) Lejopyge laevigata Biozone.

Annulum squamaceum, Comasphaeridium longispinosum and Multiplicisphaeridium martae are known from Cambrian deposits older than those in Turkey dated as latest middle Middle Cambrian. The first of these species appears at the beginning of the Lower Cambrian, before the first levels with trilobites, in the East European Platfonn (Volkova et al. 1979; Moczydlowska, 1991). Comasphaeridium longispinosum is known from Swedish boreholes, in strata palynologically correlated (Hagenfeldt, 1989) w iththq Acadoparadoxides oelandic a Biozone, conventionally the lowest subdivision of the Middle Cambrian in Scandinavia but younger than the lowest biozone in the Mediterranean region according to Geyer (1990, p. 66). At the Llÿn Peninsula, northwest Wales (Martin in Young et al. 1994), the species ranges from the Tomagnostus fissus Biozone, in the lower part of the Paradoxides paradoxissimus ‘Stage’. In the Middle Cambrian of Bohemia Multipli ci sphaeridium martae is present (F. Martin, pers. obs.) in the Jince Fonnation on the hill-slope at Vinice, close to Jince, at a level (M. Vavrdová, pers. comm., 1984) with Eccaparadoxides pusillus, index species of the lowest Middle Cambrian biozone in Bohemia; the latter could conespond (Nikolaisen & Henningsmoen, 1987, p. 77) to the E. insularis Biozone, lowest Middle Cambrian in Scandinavia. Fatka (1989) recorded AT. martae from a level in the same fonnation at Vinice Hill, later dated as Onvmagnostus hybridus Biozone, the range of which overlaps the upper part of the E. pusillus Biozone (Fatka & Kordule, 1992, p. 57, not fig. 3). These data are insufficient to establish which of the two levels with Multiplicisphaeridium martae in the Jince Fonnation is the older. In the Moroccan Anti-Atlas, and on the basis of unconfinned, preliminary trilobite detenninations, Vanguestaine & Van Looy (1983) considered that the species, as well as Timofeevia lancarae and Cristallinium cambriense, appeared in the early Middle Cambrian.

Figure 8. Specimens here and in Figure 9 have numbers with prefix IRScNB and are in the Institut royal des Sciences naturelles de Belgique, Brussels. Magnification x 1000 unless otherwise stated, (a-e, g, i, j, 1, n, q, s, t): upper part of Koruk Fonnation; (f, h, k, m, o, p, r, u-x): Sosink Fonnation. Sample numbers have prefixes T-91 and T-92. (a-e)Multiplicisphaeridium martae Cramer & Diez, 1978. T-92-TUT-23. (a) IRScNB b2657; (b) IRScNB b2658; (c) IRScNB b2659; (d) IRScNB b2660; (e) IRScNB b2661. (T)Pirea? sp. T-91- TUT-11, IRScNB b2662, x 500. (g) Dichotisphaera sp. T-92-KUC-1, IRScNB b2647. (h, 1-n, q, r, u, a)Micrhystridium lanceolatum Vanguestaine, 1974. Proximal enlarged part of processes variably contracted, (h, m) fragile, distal part of processes totally absent; (h) T-92-OM-8, IRScNB b2650; (1) T-92-KUC-31, IRScNB b2651; (m) T-92-KUC-5, IRScNB b2652; (n) T-92-KUC-31, IRScNB b2653; (q) T-92-TUT-23, IRScNB b2654; (r, u) T-92-KUC-19, IRScNB b2655; (u) enlargement, x 3000, of lower part of (r); (x) T-91-TUT-6, IRScNB b2656, x 2000. (i, j) Eliasum llaniscum Fombella, 1977. T-92-TUT-23, x 500. (i) IRScNB b2648; (j) IRScNB b2649. (k) Comasphaeridium longispinosum Hagenfeldt, 1989. T-92-KUC-2, IRScNB b2643, x 500. (o) Annulum squamaceum (Volkova) Martin in Martin & Dean, 1983. T-92-KUC-2, IRScNB b2640. (p) Cristallinium muliense (Cramer & Diez) Martin»; Martin & Dean, 1981. T- 92-TUT-23, IRScNB b2646. (s, t) Cristallinium cambriense (Slaviková) Vanguestaine, 1978. T-92-TUT-23. (s) IRScNB b2644; (t) IRScNB b2645. (v, w) Coenobial acritarch sensu Di Milia, 1991. (v) T-92-OM-8, IRScNB b2641, x 500; (w) T-92-OM-9, isolated compressed cells with central opening. IRScNB b2642

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50 W. T. D E A N A N D O THERS

Figure 9. For legend see lacing page.

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The presence of the genus Pírea? Vavrdová, 1972 at TUT-11 in the Kaplandere section is exceptional and its age there could be either latest middle or early late Middle Cambrian. Volková (1990) described the taxon from borehole deposits without macrofauna attributed to an interval extending from the upper part of the Middle Cambrian to the lower part of the Upper Cambrian in the East European Platform. It may be that Monocrodium? sp. of Di Milia (1991, pi. 2, fig. 7) from a level (sample S70) in the Solanas Sandstone of Sardinia dated as Upper Cambrian by the presence of Stelliferidium Deunff, Górka & Rauscher, 1974, belongs to Pirea. The latter is known especially from the Ordovician (Arenig-Llanvim) of Perigondwana, and its record (Fombella, 1986) from the Tremadoc of León Province, northeast Spain, is doubtful. In particular, Pirea fausta Fombella (1986) resembles a transversely septate fungal spore.

The oldest published record (Welsch, 1986) of Cristallinium ovíllense with independent age control is from Middle Cambrian strata, unit K1 of the Kistedal Fonnation, in the Digennul Peninsula, northern Norway. According to Nikolaisen & Henningsmoen (1987) the trilobites from K1 compare best with those of the Eccaparadoxides pusillus Biozone in Bohemia.

In the Penbegli-Tut inlier Micrhystridium lanceolatum enters the succession in strata without trilobites between the Pardailhania and Solenopleuropsis biozones, and ranges higher than Solenopleuropsis. It occurs in borehole assemblages palynologically dated as middle Middle Cambrian in the East European Platfonn (Assemblage SKI, Volkova, 1990) and the Stavelot Massif, Belgium (Zone 3, Vanguestaine, 1974,1978).

Timofee\’ia manota seems to occur earlier on the margin of the Arabian Platfonn, in Turkey, than in the Rhadames Basin, western Libya. The species was described from a borehole in northern Tripolitania, where it is found at the same level as T. pentagonalis and slightly before the entry of Vulcanisphaera turbata, at the lower limit of microflora GB2 described by Albani, Massa & Tongiorgi (1991). In the absence of independent age control, these authors conelated the assemblage with a selected part of an interval represented by the T. pentagonalis-]’ turbata Biozone, in the upper part of microflora A2 in eastern Newfoundland, which they considered to correspond to the early Late Cambrian.

The record of the coenobial acritarchs is certainly more precocious in Turkey than in Sardinia, where Di Milia (1991) described them from the same sample (S70, from the Riu San Giorgio) as that containing Monocrodium? sp.

Acknowledgements. Our fieldwork in the inlier was supported by Turkish Petroleum Corporation (T.P.A.O.), who kindly permitted publication of our results and of their previously unpublished maps. Monod acknowledges support from C.N.R.S. (URA 1366) and computer drawing by Nathalie Laurent- Rouchon, and Dean thanks the Leverhulme Trust for support in preparation of the manuscript. At the Institut royal des Sciences naturelles de Belgique, Brussels, Martin thanks Hugo de Potter for treatment of the palynological samples, Julien Cillis for SEM manipulation, and Wilfried Miseur for photographic prints.

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Figure 9. Magnification x 1000 unless otherwise stated, (a-e, j, k, n): upper part of Komk Fonnation; (f-i, 1, m, o): Sosink Fonnation. (a, b, d, e) Timofeevia manato Albani et cd. 1991. T-92-KUC-1. (a, d) IRScNB b2668; (d) enlargement, x 3000, of middle left part of (a), (b, e) IRScNB b2669; (e) enlargement, x 3000, of lower left part of (b). (c, i) Timofeevia phosphoritica Vanguestaine, 1978. (c) T- 92-TUT-23, IRScNB b2670; (i) T-91-TUT-11, x 750; upper, IRScNB b2671; lower, IRScNB b2672. (f, g, m-o) Timofeevia lancarae (Cramer & Diez) Vanguestaine, 1978. (f) T-91-TUT-3, IRScNB b2663; (g) T-92-KUC-19, IRScNB b2664; (m) T-92-KUC-17, IRScNB b2665; (n) T-92-TUT-23, deformation by pyrite, IRScNB b2666; (o) T-91-TUT-3, IRScNB b2667. (h, j-1) Transition Timofeevia lancarae—T. phosphoritica, (h) T-92-KUC-19, IRScNB b2673; (j, k) T-92-TUT-23, IRScNB b2674; (k) enlargement, x 3000, of upper left part of (j); (1) T-91-TUT-3, IRScNB b2675.

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Appendix. Location of microfossil samples

Sample numbers listed in descending stratigraphie order. A, acritarchs abundant, well preserved; a, acritarchs rare, well preserved; (a) acritarchs rare, poorly preserved; o, acritarchs undeterminable or absent.

1. West end of Kaplandere, and area immediately to westSosink Formation

highest part of section; close to FOB-71 ( = Holasaphus mesopotamicus level)T-91-TUT-3: 2.00 m above FOB-71, A T-92-TUT-30: 2.00 m below FOB-71, A

no zonal trilobites; post-Solenopleuropsis interval T-91-TUT-11: 89.60 m above base of fonnation, AT-91-TUT-10: 50.90 m above base of fonnation, AT-91 -TUT-9: 35.90m above base of fonnation, aT-91-TUT-7: 16.00 m above base of fonnation, AT-92-OM-9: 15.00 m (est.) above base of fonnation, A

no zonal trilobites; interval between Pardailhania and Solenopleuropsis biozonesT-91-TUT-4: 9.40 m above base of fonnation, AT-91 -TUT-2 8: 6.30m above base of fonnation, AT-91-TUT-27: 5.00 m above base of fonnation, AT-92-OM-8: 5.00 m (est.) above base of fonnation, AT-92-TUT-26: 3.00 m above base of fonnation, A

Kornii Formationno zonal trilobites; interval between Pardailhania and

Solenopleuropsis biozonesT-92-TUT-2 F 0.60 m below top of fonnation, aT-91-TUT-6: 1.40 m belowtop of fonnation, AT-92-TUT-22: 1.60 m belowtop of fonnation, AT-92-TUT-23: 2.20 m belowtop of fonnation, AT-92-TUT-24: 3.05 m belowtop of fonnation, AT-92-TUT-25: 4.05 m belowtop of fonnation, oT-91 -TUT-5: 100 m (est. ) below top of fonnation, o

2. Devret A sectionSosink Formation Solenopleuropsis BiozoneT-92-KUC-40: 3.50 m above base of fonnation, A

Koruk Formationno zonal trilobites; 8 m below Solenopleuropsis Biozone

T-92-KUC-39: 3.50 m belowtop of fonnation, A

3. Devret B sectionSosink Formation

no zonal trilobites; post-Solenopleuropsis interval307.00237.00189.90187.90177.80 168.20165.50150.80136.50 125.70120.50

m (est. ) above base of fonnation, A m (est.) above base of fonnation, (a) m above base of fonnation, A m above base of fonnation, A m above base of fonnation, A m above base of fonnation, A m above base of fonnation, A m above base of fonnation, A m above base of fonnation, A m above base of fonnation, A m above base of fonnation, a

T-92-KUC-23 T-92-KUC-24 T-92-KUC-21 T-92-KUC-38 T-92-KUC-19 T-92-KUC-18 T-92-KUC-17 T-92-KUC-15 T-92-KUC-13 T-92-KUC-12 T-92-KUC-11

Solenopleuropsis T-92-KUC-10 T-92-KUC-54 T-92-KUC-36 T-92-KUC-8:T-92-KUC-53:T-92-KUC-6 T-92-KUC-5 T-92-KUC-3 T-92-KUC-2

Koruk Formation Solenopleuropsis BiozoneT-92-KUC-32: 0.35 m belowtop of fonnation, AT-92-KUC-31: 0.75 m below top of fonnation, AT-92-KUC-1: 2.35 m belowtop of fonnation, A

4. Area east of MeryemuçagiMeryemuçagi FormationTUT-12, 13 and 15 are from the northeast side of the Tut-Meryemu§agi road (Fig. 2), east of its junction with the unmade road to Çanakci, which serves as a marker point. The localities are, respectively, 14 m, 24 m and 63 m east of the junction, and 0 m, 3 m and F5 m above road level. No acritarchs detennined, but organic debris abundant.

Biozone113.80m above base of fonnation, A106.00 m above base of fonnation, A 103.60 m above base of fonnation, a 9F30 m above base of fonnation, a 90.20 m above base of fonnation, (a)80.50 m above base of fonnation, A79.50 m above base of fonnation, A48.00 m above base of fonnation, A14.50 m above base of fonnation, A

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