2022 | 75/1 | 115–128 | 9 Figs. | 1 Tab. | 2 Pls. | www.geologia-croatica.hr Journal of the Croatian Geological Survey and the Croatian Geological Society The radiolarian age and petrographic composition of a block of the Lower Jurassic volcaniclastic breccia and chert of the Mamonia Complex, SW Cyprus Nikita Bragin1, Galina Ledneva1, Liubov Bragina1, Efthymios Tsiolakis2, Vasilis Symeou2 and Nikolaos Papadimitriou2 1Geological Institute of Russian Academy of Sciences, Moscow, 119017, Russia, (*corresponding author: bragin.n@mail.ru) 2Cyprus Geological Survey Department P.O.Box 24543, 1301 Lefkosia, Cyprus doi: 10.4154/gc.2022.07 Abstract An exceptional exposure of volcaniclastic breccia intercalated with radiolarian cherts and lime- stones was studied which constitutes a unique block within the Upper Cretaceous Mamonia Mélange in the Akamas Peninsula of southwestern Cyprus. This breccia, represents the lower part of the sedimentary cover of the Upper Triassic Phasoula Formation volcanics. The breccia mainly consists of clasts of metabasalts, diabases, metagabbros, hyaloclastites and quartz-al- bite-chlorite-epidote aggregates, which have been metamorphosed at greenschist facies, and subordinate siltstones. The thin-bedded cherts intercalated between breccia levels, yielded ra- diolarian assemblages, which indicate an Early Jurassic age (Sinemurian to Pliensbachian) for the sequence. 1. INTRODUCTION The geology of southwestern Cyprus is characterized by exten- sive occurrences of Mesozoic allochthonous rock assemblages that were grouped together as the Mamonia Complex (GASS, 1960; LAPIERRE, 1975; ROBERTSON & WOODCOCK, 1979; SWARBRICK & ROBERTSON, 1980; MALPAS et al., 1992). The Mamonia Complex is divided in two major sub-groups, the Ayios Photios Group and the Dhiarizos Group, including exten- sive zones of tectonic mélange known as the Mamonia Mélange (Fig. 1). The Ayios Photios Group (SWARBRICK & ROBERT- SON, 1980) consists of Upper Triassic to Upper Cretaceous sedi- mentary units (BRAGIN & KRYLOV, 1996; 1999; BRAGIN et al., 2000; BRAGINA & BRAGIN, 2016), while the Dhiarizos Group (SWARBRICK & ROBERTSON, 1980) is composed of Upper Triassic to Lower Cretaceous basic volcanic rocks and their sedimentary cover. The Mamonia Mélange consists of a sedimentary matrix of highly tectonized siltstones and mud- stones of the Ayios Photios Group, mixed with different-sized blocks from various lithologies of the Mamonia Complex and to a lesser extent from the Troodos Ophiolite (GEOLOGICAL SUR- VEY DEPARTMENT OF CYPRUS, 2008; 2015). The age determination of the Mesozoic sedimentary se- quences of the Mamonia Complex is estimated from the presence of radiolarian chert and cherty mudstone layers within these de- posits, indicating that the radiolarian biostratigraphy is of signifi- cant importance for the dating of these deep-water lithologies, which lack other macrofossils or foraminifers. This article presents new petrographic and palaeontological data from a sedimentary-volcaniclastic breccia block that pre- sumably represents the lower part of the sedimentary cover of the Dhiarizos Group. This work represents the first time that this type of Lower Mesozoic sedimentary-volcaniclastic breccia, of south- western Cyprus, is studied from a micropalaeontological/bio- stratigraphical perspective. 2. GEOLOGICAL SETTING Two main Mesozoic rock complexes are widespread in south- western Cyprus: the Troodos Ophiolite Complex and the Mamo- nia Complex (Fig. 2A). Both are allochthonous and form systems of nappes, the relationship between them is strictly tectonic. The Mesozoic complexes of Cyprus reflect the history of the southern branch of Neotethys. The Mamonia Complex represents the Up- per Triassic to Cretaceous deposits and Upper Triassic volcanics of the northern margin of Gondwana, whereas the Troodos Com- plex constitute Cretaceous oceanic formations. Both complexes became juxtaposed in the Late Cretaceous with the development of the nappe system with chaotic assemblages (mélanges and oli- stostromes). The Troodos Ophiolite Complex is a fully developed frag- ment of oceanic lithosphere that consists of lithologies ranging from upper mantle harzburgites to pillow lavas, overlain by um- bers (hydrothermal sediments) with radiolarian cherts of the up- per Turonian to uppermost Santonian Perapedhi Formation (WIL- SON, 1959; SWARBRICK & ROBERTSON, 1980; BLOME & IRWIN, 1985; BRAGINA & BRAGIN, 1996; BRAGINA, 2012; 2016). The latter are locally capped by a sedimentary sequence consisting of Campanian to middle Maastrichtian bentonitic clays and volcaniclastic sandstones and siltstones of the Kannaviou For- mation (ROBERTSON & HUDSON, 1974; ROBERTSON, 1977). The Mesozoic lithologies of the Mamonia Complex are mainly grouped into the Ayios Photios Group (sedimentary) and the Dhiarizos Group (volcano-sedimentary), (ROBERTSON & WOODCOCK, 1979; SWARBRICK & ROBERTSON, 1980), which are subdivided into a number of sub-units (Fig. 1). The Ayios Photios Group consists of the following sub-units: the Vlampouros Formation (Upper Triassic siliciclastics and micritic limestones with minor chert interlayers) (SWARBRICK & ROB- ERTSON, 1980; BRAGIN & KRYLOV, 1996; TORLEY & ROB- ERTSON, 2018) and the Episkopi Formation (Middle Jurassic to Article history: Received June 02, 2021. Revised manuscript accepted November 10, 2021 Available online February 22, 2022 Keywords: sedimentary-volcaniclastic breccia, metavolcanics, Lower Jurassic, Radiolaria, Cyprus G eo lo gi a C ro at ic a 116 Geologia Croatica 75/1 middle Cretaceous, Albian–Turonian, alternating layers of cherts, mudstones, limestones, sandstones, siltstones and clays) (SWARBRICK & ROBERTSON, 1980; BRAGIN & KRYLOV, 1999; BRAGIN et al., 2000). The thick Lower Cretaceous sand- stones within the Episkopi Formation are referred to as the Aka- mas Member or the Akamas Sandstone (SWARBRICK & ROB- ERTSON, 1980). Several authors in previous studies have included within this group another sub-unit, referred to as the Marona For- mation to describe blocks of Upper Triassic hemipelagic lime- stones (SWARBRICK & ROBERTSON, 1980; TORLEY & ROB- ERTSON, 2018). The Dhiarizos Group consists of the following sub-units: the Phasoula Formation (Upper Triassic basic volcanics with inter- layers of limestones and cherts) (SWARBRICK & ROBERTSON, 1980; BRAGIN, 2007; 2010), the Loutra tis Aphroditis Formation (Upper Triassic lava breccias and volcaniclastic breccias with in- terlayers of volcaniclastic siltstones and radiolarian mudstones) (SWARBRICK & ROBERTSON, 1980), the Petra tou Romiou Formation (detached blocks of Upper Triassic reefal limestones) (HENSON et al., 1949; SWARBRICK & ROBERTSON, 1980; MARTINI et al., 2009), and the Mavrokolympos Formation (Ju- rassic to Cretaceous alternating layers of limestones, cherts, mud- stones, siltstones and calcilutites) (SWARBRICK & ROBERT- SON, 1980). The sedimentary interlayers within and above the Phasoula and Loutra tis Aphroditis formations are referred to as the Kholetria Member and are represented by chert-limestone al- ternations (SWARBRICK & ROBERTSON, 1980). Furthermore, the greenschist- to amphibolite-facies metamorphic rocks are termed the Ayia Varvara Formation (metasediments and metavol- canics of various Dhiarizos lithologies, metamorphosed during the Cretaceous) (MALPAS et al., 1992; CHAN et al., 2007; 2008). For the purposes of this study, field work was conducted in the southwestern part of the Akamas Peninsula (Fig. 2). This area is characterized by the extensive distribution of the Ayios Photios Group lithologies and the Mamonia Mélange. Furthermore, seve- Figure 1. Generalized chart of the stratigraphy of the Mamonia Complex. The grey area shows the Kholetria Member within and above the Phasoula Forma- tion. For other lithologies and references see text. Figure 2. A – position of the study area in western Cyprus. B – Generalized geological map of the area east of Lara Bay (Akamas Peninsula, Cyprus) (GEOLOGICAL SURVEY DEPARTMENT OF CYPRUS, 2015). G eologia C roatica 117Bragin et al.: The radiolarian age and petrographic composition of a block of the Lower Jurassic volcaniclastic breccia and chert of the Mamonia ... ral big blocks of the Dhiarizos Group (mainly the Phasoula For- mation) are also observed within the Mamonia Mélange. These blocks are mainly composed of basic volcanics commonly with interbeds of limestone and radiolarian chert. One of these blocks is composed of sedimentary-volcaniclastic breccia consisting mainly of fragments of basalts, diabases and gabbro, with inter- layers of limestones and cherts that yield abundant radiolarian assemblages. This roughly rounded block is located 2.5 km east-northeast of the northern Lara Bay (Fig. 2) and has an extent of 270 x 200 m, with an elongated axis along a SW – NE direction (Fig. 3, Fig. 4A, B). The studied breccia block is in tectonic contact with the surrounding matrix of the Mamonia Mélange, that yields numerous small blocks of Lower Cretaceous Akamas Sandstone of the Episkopi Formation (SWARBRICK & ROBERTSON, 1980) (Fig. 4C), Upper Triassic limestones of the Petra tou Ro- miou Formation or the Kholetria Member (SWARBRICK & ROBERTSON, 1980), as well as basic volcanics of the Upper Tri- assic Phasoula Formation. The matrix of the mélange consists of reddish-grey to brownish-grey mudstones and siltstones. Further- more, another, smaller block of similar breccia was identified near the NW boundary of the studied breccia block (Fig. 3, sampling location 18-19). From the detailed survey of the large breccia block, from the northwestern boundary (point 18-18, coordinates 34⁰ 58’ 22,4’’ N, 32⁰ 20’ 13,4’’ E) towards its southern edge (point 18-15, coor- dinates 34⁰ 58’ 17,5’’ N, 32⁰ 20’ 19,9’’ E) (Fig. 3, 4, 5, 6), various individual units of the block were recognized and described: 1. Greenish-grey hard cemented breccia mainly consisting of small (3-5 up to 15-20 cm in size) diabase and subor- dinate metagabbro clasts in a coarse-grained to gravelly matrix of the same composition. The thickness of the unit is 50 m. 2. Greenish-grey and reddish-brown hard cemented breccia of metabasalt, diabase and metagabbro clasts with rare small fragments of red recrystallized limestone in a coarse-grained to gravelly matrix of metabasalt, diabase and metagabbro. Lenses (1-2 m thick) of breccia within a pinkish matrix of highly brecciated limestone, occur in the upper part of the unit. The thickness of the unit is 100 m. 3. Pink to greenish-brown hard cemented breccia of diabase and metabasalt clasts within a matrix of highly brecci- ated pink to white limestone (Fig. 4F). The thickness of the unit is 4 m. 4. Greenish-grey hard cemented breccia with lenses (1,5 m thick) of breccia within a matrix of highly brecciated pink to white limestone (Fig. 4E). The thickness of the unit is 20 m. 5. White to pink, hard, thin-bedded recrystallized lime- stones with calcite veins (Fig. 5F). The thickness of the unit is 2 m. 6. Greenish-grey hard cemented breccia consisting of me- tabasalt, diabase and metagabbro fragments and blocks (Fig. 4G, H) in a coarse-grained to gravelly matrix of the same composition. The thickness of the unit is 5 m. 7. Brick-red and crimson-red, thin-bedded radiolarian cherts (Fig. 5D) with interbeds (0,5 – 1 m) of pink and white hard recrystallized limestones (Fig. 5E). The thick- ness of the unit is 20 m. 8. Greenish-grey to reddish-brown, hard cemented breccia consisting of diabase and metagabbro fragments and blocks as well as rare fragments of siltstones in a coarse- grained to gravelly matrix of the metabasalt, metagabbro and diabases. The thickness of the unit is 5 m. 9. Brick-red, thin-bedded radiolarian cherts intercalated with red cherty mudstones. Interbeds (up to 1 m) of dark- Figure 3. Detailed map of the block of diabase-gabbro breccia. A – matrix of the Mamonia Mélange; B – diabase-gabbro breccia; C – beds of limestone and radiolarian chert within the breccia; D – blocks of the Petra tou Romiou limestone; E – blocks of the Akamas sandstone; F – blocks of basic volcanics; G – fault within a block of diabase-gabbro breccia; H – positions of sampling and studying points. G eo lo gi a C ro at ic a 118 Geologia Croatica 75/1 Figure 4. Volcaniclastic breccia of the Akamas Peninsula. Outcrops of breccia. A – Block of the breccia, view from the south; B – Same block, view from the east; C – Contact between the breccia (left) and the Mamonia Mélange (right, with scattered blocks of Akamas Sandstone); D – breccia composed of small diabase and me- tabasalt clasts in a volcaniclastic matrix (unit 10); E – breccia with carbonate (calcite) matrix (unit 4); F – breccia with well-developed carbonate matrix represented by pink micritic limestone (unit 3); G – block of metagabbro (unit 6); H – blocks of diabase (unit 6). G eologia C roatica 119Bragin et al.: The radiolarian age and petrographic composition of a block of the Lower Jurassic volcaniclastic breccia and chert of the Mamonia ... greenish-grey breccia with fragments of metabasalt and metagabbro and lenses of pink recrystallized brecciated limestone are observed in the middle part of this unit. The contact between the chert and breccia layers is clearly sedimentary (Fig. 5A-C). The thickness of the unit is 5 m. 10. Dark-greenish-grey hard cemented breccia composed of unsorted diabase and metabasalt fragments in a coarse- grained to gravelly matrix of the same composition (Fig. 4D). The thickness of the unit is 6 m. It is herein assumed that this fragmentary section is the lower part of the sedimentary cover of the Upper Triassic volcanics of the Dhiarizos Group, which consists of breccia, while the upper part of the succession is characterized by the presence of lime- stone and radiolarian chert layers that become more and more abundant towards the top. 3. MATERIALS AND METHODS Twenty-five samples of various rock types including metavolcan- ics, limestones and cherts were collected during fieldwork in 2018 and 2019. The petrography of the acquired rock samples was stud- ied in standard thin-sections using a light microscope Olympus BS51. Radiolarians were extracted from chert samples using di- luted (5%) hydrofluoric acid (HF) for twelve (12) hours and the residues were rinsed with water and dried. The residues were studied using a light microscope LOMO-MBS-10. The microfos- Figure 5. Volcaniclastic breccia of the Akamas Peninsula. Outcrops of sedimentary units (chert and limestone) between breccia. A – Red radiolarian cherts and white limestones in direct contact with breccia (units 9 and 10); B – Sedimentary contact between breccia and radiolarian chert. Small lense of breccia within radiolarian cherts (unit 9); C – radiolarian cherts, a fault is visible in the left side of the photograph (unit 9); D – radiolarian cherts and bed of limestone (unit 7); E – strongly brecciated white to pink limestone (unit 7); F – thin-bedded tectonized and brecciated pink to white limestone (unit 5). G eo lo gi a C ro at ic a 120 Geologia Croatica 75/1 sils were collected, mounted, studied in detail and photographed with scanning electron microscopes: TESCAN 2300 in the Geo- logical Institute RAS, Moscow, and TESCAN VEGA-II XMU in the Palaeontological Institute RAS, Moscow. Thin sections and radiolarian assemblages are stored in the Geological Institute RAS, Moscow, Russia. 4. PETROGRAPHY 4.1. Breccia with carbonate matrix The breccia consists of metabasalt, diabase and metagabbro blocks and clasts that are irregularly shaped, sub-angular and poorly sorted. These rock fragments vary from a few centimetres to 10-15, rarely 20-30 cm in size. The matrix is represented by micritic limestone or recrystallized calcite. 4.1.1. Breccia clasts Metabasalts are represented by amygdaloidal aphyric, plagio- clase- and clinopyroxene-plagioclase porphyric varieties (Fig. 7A, B, 8A, B). Phenocrysts of clinopyroxene are represented by short-prismatic crystals (0.4-0.9 mm) and are partly replaced by amphibole. Phenocrysts of plagioclase are tabular and often elon- gated tabular zoned crystals (0.2 mm); plagioclase is completely altered pseudomorphs of albite, epidote group mineral and chlo- rite creating a very fine-grained aggregate. The groundmass ex- hibits hyalopilitic and intersertal textures. The intersertal ground- mass is composed of altered plagioclase, altered pyroxene and opaque minerals; the hyalopilitic groundmass is composed of elongated, needle-shaped, often skeletal plagioclase and altered glass replaced by a black opaque substance. Diabase (Fig. 7C) is composed of pseudomorphs after the altera- tion of plagioclase and pyroxene crystals, Fe-Ti oxides, quartz and micrographic intergrowths of quartz with feldspar. Plagio- clase pseudomorphs are nearly euhedral in form, elongated tabu- lar grains of a microcrystalline aggregate of epidote, colourless chlorite and albite in cores or rims. Pyroxene pseudomorphs are nearly euhedral and anhedral grains, represented by light-green to colourless amphibole with tiny inclusions of titanite. Fe-Ti ox- ides, which are abundant in the rock, comprise euhedral crystals with lacy edges. Minor quartz (<1%) and its intergrowths with feldspar (<1%) fill interstices. The rock texture is doleritic. 4.1.2. Carbonate matrix The matrix is represented mainly by pink to white micritic lime- stone which is often strongly brecciated and cut by calcite veins (Fig. 8A, B). This matrix yields small non-sorted clasts of meta- basalts and chlorite (formed supposedly after volcanic glass). Sometimes, the matrix is represented by highly recrystallized calcite. There is no visible layering of the matrix. Rare epidote group minerals are present in the carbonate matrix between clasts (Fig. 7B). 4.2. Breccia with sandstone-gravel matrix This type of breccia is composed of metabasalt, diabase and meta- gabbro blocks, altered volcanic glass, quartz-albite-chlorite-epi- dote aggregates and rarely siltstone clasts. Blocks and clasts are irregularly shaped, sub-rounded and poorly sorted rock frag- ments from predominantly few centimetres up to 20-30 cm in size. The matrix is represented by sandstone-gravel that has the same composition with the large (both rock and mineral debris) clasts. Breccia clasts Metabasalts and diabase are represented by the same lithologies as clasts of the breccia with carbonate matrix. Metagabbro (Fig. 7D) is composed of clinopyroxene, pseudo- morphs after the alteration of plagioclase and an accessory opaque mineral. Clinopyroxene is preserved only in relicts and is largely replaced by green to light-yellow amphibole with lamel- lae of an opaque mineral (<100 µm in size) and chlorite with in- terference in a blue colour. Plagioclase pseudomorphs form eu- hedral tabular grains, composed of a microcrystalline aggregate of albite, an epidote group mineral and chlorite. The opaque mine- ral is anhedral. Metagabbro is a fine- to medium-grained rock exhibiting a primary hypidiomorphic-granular texture. Some clasts exhibit no primary textures. Intensively frac- tured clasts of presumably altered volcanic glass (Fig. 7E) con- sist of pale-green and colourless chlorite with minor hydrogarnet and fine- to medium-grained aggregates of quartz, albitite, epi- dote group mineral and chlorite which are produced from an un- identified rock. Figure 6. Stratigraphic column of volcaniclastic breccia with interbeds of limestones and cherts. A – breccia with volcaniclastic matrix; B – breccia with carbonate matrix; C – limestone; D – radiolarian chert; E – position of samples with radiolarians and their numbers. Numbers of units according to the descrip- tion are shown to the right of the column. G eologia C roatica 121Bragin et al.: The radiolarian age and petrographic composition of a block of the Lower Jurassic volcaniclastic breccia and chert of the Mamonia ... Figure 7. Clasts typical of breccia. A – plagioclase-pyroxene porphyric basalts with intersertal groundmass (sample 18-17-6, unit 4); B – clasts of amygdaloidal aphyric basalt with a hyalopilitic groundmass and chlorite presumably after volcanic glass in carbonate matrix (sample 18-17-3, unit 4); C – diabase (metadolerite), enriched by ore minerals (sample 18-16-2, unit 8); D – metagabbro with plagioclase replaced by albite, zoisite and chlorite, and with clinopyroxene replaced by amphibole (sample 18-20-2, unit 1); E – fractured clast of chlorite with minor hydrogarnet presumably after volcanic glass in sandstone matrix dominated by quartz and plagioclase (sample 18-15-2, unit 10); F – clasts of siltstone and aggregate of quartz, albite, epidote group mineral and chlorite (sample 18-15-3, unit 10); G – detail of siltstone clast, polarized light (sample 18-15-3, unit 10); H – detail of siltstone clast (sample 18-15-3, unit 10). G eo lo gi a C ro at ic a 122 Geologia Croatica 75/1 Siltstone clasts (sample 18-15-2, unit 10, Fig. 7F-H) are com- posed of quartz and feldspar (albite). The supporting matrix is composed of chlorite and an epidote group mineral. Thin frac- tures are filled by carbonate minerals. Sandstone-gravel matrix Sandstone-gravel matrix is represented by the same litholo- gies as in the blocks and clasts. The matrix exhibits no layering or sorting. Occasional veins of calcite are present. 4.3. Limestone and radiolarian chert beds and lenses within the breccia succession Limestones and radiolarian cherts form interbeds and lenses within the breccia. Limestones are represented by micrites which are commonly brecciated, and sometimes contain recrystallized radiolarian remains. Stylolites and fractures filled by calcite are common; these fractures are commonly confined to limestone clasts (Fig. 8C, D). Red radiolarian cherts usually yield abundant, moderately, to poorly preserved radiolarian assemblages. Fractures are filled by quartz (Fig. 8E, F). 5. RADIOLARIAN ASSEMBLAGE AND AGE OF BRECCIA Abundant radiolarians are present in the chert beds of the upper part of the studied section (Plate 1, 2, localities 18-15 and 18-16). The systematic composition of the radiolarian assemblages re- Figure 8. Sedimentary rocks intercalated with breccia. A – brecciated limestone with rare clasts of aphyric and plagioclase porphyry metabasalts, and chlorite supposedly after volcanic glass. Fractures filled with calcite cut both matrix and clasts (sample 18-17-5, unit 4); B – limestone with clast of plagioclase porphyry metabasalt with intersertal groundmass (sample 18-17-5, unit 4); C, D – brecciated micritic limestones with relics of radiolarians (sample 18-15-1, unit 9); E – red radiolarian chert with moderately preserved radiolarians (sample 18-15-7, unit 9); F – dark-red radiolarian chert with abundant, moderately to poorly preserved radiolarians (sample 18-6-6, unit 7). G eologia C roatica 123Bragin et al.: The radiolarian age and petrographic composition of a block of the Lower Jurassic volcaniclastic breccia and chert of the Mamonia ... covered from units 7 and 9 (Fig. 6) is similar (Table 1). The prese- nce of several characteristic taxa within the radiolarian assem- blages is used to determine the age of the radiolarian cherts ( Fig. 9). Primary attention was given to well-preserved radiolarians determined to the species level useful for dating. Taxa described in open nomenclature are of secondary importance. Sample 18-15-6 This sample yielded an abundant and diverse assemblage that al- lowed successful dating (Fig. 9, Table 1). Bagotum maudence PESSAGNO & WHALEN is present in the upper Sinemurian – lower Toarcian of Canada (PESSAGNO & WHALEN, 1982; CARTER ET AL., 2010), in the lower Toar- cian of Japan (YAO, 1997), and in the upper Pliensbachian of Oman (BLEICHSCHMIDT et al., 2004). The presence of this species in the upper Sinemurian is documented on Kunga Island (Haida Gwaii) in the Sinemurian part of the Sandilands Forma- tion together with the ammonite Tetraspidoceras sp. (see fig. 3 in (CARTER et al., 2010)). The range of species according to the present data is upper Sinemurian – lower Toarcian. Beatricea argescens (CORDEY) is known from the Pliens- bachian of British Columbia, Canada (CORDEY, 1998; GORIČAN et al., 2006) and from the Lower Jurassic of Japan and New Zealand (GORIČAN et al., 2006). Bipedis hannai WHALEN & CARTER, 1998 is known from the lower Hettangian – lower Sinemurian of Canada (CARTER et al., 1998), from the lower Sinemurian of the Philippines (YEH & CHENG, 1998) and from the Hettangian – Sinemurian of Tur- key (TEKIN, 2002). The known range of the species is Hettan- gian – lower Sinemurian, but it needs additional study because it is proven by macrofossils only in Haida Gwaii, British Columbia, Canada (CARTER et al., 1998). Bipedis japonicus GORIČAN et al., 2006 was firstly re- ported from the Hettangian to the Pliensbachian of Japan (HORI, 1990). It was documented later in the lower Pliensbachian of Can- ada (CARTER et al., 2010). Due to the absence of macrofossils in the Lower Jurassic chert sequences of Japan, we can state that the range is from the Hettangian to Pliensbachian under question. Gorgansium gongyloideum (KISHIDA & HISADA) is a worldwide known species with a large stratigraphic range – from the Rhaetian (Upper Triassic) to the middle Toarcian (CIFER et al., 2020; TEKIN et al., 2020). Katroma ninstintsi CARTER is known from the Pliens- bachian of Canada (CARTER et al., 1988; CARTER et al., 2010), the Philippines (YEH & CHENG, 1998), Austria (GAWLICK et al., 2001; CIFER et al., 2020), Turkey (TEKIN, 2002), and East- ern Russia (BRAGIN & BRAGINA, 2017). Pantanellium sixi WHALEN & CARTER, 1998 is known from the upper Sinemurian of Canada (CARTER et al., 1998). This species is known from only one region, and its stratigraphic range needs additional study. Paronaella grahamensis CARTER was reported from nu- merous localities: from the lower Pliensbachian to the Aalenian of Canada (CARTER et al., 1988; CARTER et al., 2010), from the Pliensbachian of Mexico (WHALEN & CARTER, 2002), Greece Table 1. Taxonomic composition of studied samples of radiolarian cherts. A – abundant, C – common, R – rare. Radiolarian taxa Samples 18-15-6 18-15-7 18-15-8 18-16-7 Bagotum maudense PESSAGNO & WHALEN R Beatricea sp. cf. B. christovalensis WHALEN & CARTER R Beatricea sp. C R R Bipedis hannai WHALEN & CARTER R C Bipedis patricki WHALEN & CARTER R R C Canoptum sp. cf. C. anulatum PESSAGNO & POISSON R Canoptum sp. cf. C. artum YEH R Charlottea weedensis WHALEN & CARTER R Gorgansium gongyloideum KISHIDA & HISADA A C C C Gorgansium morganense PESSAGNO & BLOME R Katroma sp. cf. K. irwingi WHALEN & CARTER R R C Katroma ninstintsi CARTER C R C Lantus sp. R Pantanelluim sixi WHALEN & CARTER A R R Paronaella grahamensis CARTER C C Paronaella sp. cf. P. notabilis WHALEN & CARTER R Praehexasaturnalis tetraradiatus KOZUR & MOSTLER R Pseudoeucyrtis busuangaensis (YEH & CHENG) R C Pseudoeucyrtis sp. cf. P. busuangaensis (YEH & CHENG) R R Udalia sp. cf. U. primaeva WHALEN & CARTER R Figure 9. Stratigraphic ranges of selected radiolarian taxa and proposed dating of the breccia unit. G eo lo gi a C ro at ic a 124 Geologia Croatica 75/1 (CHIARI et al., 2013), Eastern Russia (BRAGIN & BRAGINA, 2017), and Austria (CIFER et al., 2020). The range of this species is from the Pliensbachian to the Aalenian. Praehexasaturnalis tetraradiatus KOZUR & MOSTLER is present in the Hettangian of Germany (KOZUR & MOSTLER, 1990), and Canada (CARTER et al., 1998; CARTER & HORI, 2005; LONGRIDGE et al., 2007), the Pliensbachian of Mexico (WHALEN & CARTER, 2002), the Hettangian to Sinemurian of Turkey (TEKIN, 2002), and the lower Pliensbachian of Austria (CIFER et al., 2020). The range is Hettangian to lower Pliens- bachian. Pseudoeucyrtis busuangaensis (YEH & CHENG) is known from the Lower Jurassic of the Philippines (YEH & CHENG, 1998), Japan (HORI, 2004), and Oman (BLEICHSCHMIDT et al., 2004). Recently it is documented from the lower Sinemurian – lower Pliensbachian of Turkey (TEKIN et al., 2020). Udalia primaeva WHALEN & CARTER, 1998 is present in the Hettangian and lower Sinemurian of Canada (CARTER et al., 1998) and from the Hettangian to the Sinemurian of Turkey (TEKIN, 2002). The range of this species needs additional study. Certain contradictions between the stratigraphic ranges of the radiolarian taxa are observed. For example, the last appear- ance data of Bipedis hannai WHALEN & CARTER is upper Sinemurian, whereas the first appearance data of Katroma nin- stintsi CARTER and Paronaella grahamensis CARTER are lower Pliensbachian. The age determination of this assemblage as it is, is estimated with caution as Sinemurian–Pliensbachian. Sample 18-15-7 This sample yielded only few taxa determined at species level (Fig. 9, Table 1). These are: Bipedis japonicus GORIČAN et al., 2006 (Hettangian? – Pliensbachian?), Gorgansium gongyloideum (KISHIDA & HISADA) (Rhaetian – middle Toarcian), Katroma ninstintsi CARTER (Pliensbachian), and Pantanellium sixi WHALEN & CARTER (upper Sinemurian). This poses a similar contradiction: between the ranges of Katroma ninstintsi and Pan- tanellium sixi. The age of the sample can be supposed to be Sine- murian – Pliensbachian. Sample 18-15-8 Only three species are represented here, two of them were deter- mined in open nomenclature (Fig. 9, Table 1): Gorgansium gon- gyloideum KISHIDA & HISADA, Katroma sp. cf. K. irvingi WHALEN & CARTER and Pseudoeucyrtis sp. cf. P. busuan- gaensis (YEH & CHENG). Their presence confirmed the Early Jurassic age of the sample, but did not allow more detailed dating. Sample 18-16-7 This sample yielded a diverse and moderately well-preserved as- semblage which slightly differs from sample 18-15-6. Canoptum? megathelus CORDEY is present in the Lower Jurassic of Canada (CORDEY, 1998). The stratigraphic impor- tance of this species is poorly known. Charlottea weedensis WHALEN & CARTER, 1998 was previously reported from the Hettangian and lower Sinemurian of Canada (CARTER et al., 1998), from the Middle Jurassic (Ba- thonian) of Oregon (YEH, 2009), and from the Hettangian – Sine- murian of Turkey (TEKIN, 2002). It seems that this species has a broad stratigraphic range – from the Hettangian to the Batho- nian. Gorgansium morganense PESSAGNO & BLOME is known from the lower Pliensbachian of British Columbia (CARTER et al., 2010) and Oregon (PESSAGNO & BLOME, 1982; YEH, 1987). The stratigraphic range is questionable, because this spe- cies is studied only in two regions of North America. Other species are the same as in sample 18-15-6: Bipedis hannai WHALEN & CARTER (Hettangian – Sinemurian), Bi- pedis japonicus GORIČAN et al., 2006 (Hettangian? – Pliens- bachian?), Gorgansium gongyloideum KISHIDA & HISADA (Rhaetian – middle Toarcian), Katroma ninstintsi CARTER (Pliensbachian), Pantanellium sixi WHALEN & CARTER (up- per Sinemurian), Paronaella grahamensis CARTER (Pliens- bachian – Aalenian), and Pseudoeucyrtis busuangaensis (YEH & CHENG) (lower Sinemurian – lower Pliensbachian). As a result, we have for this sample clear contradictions be- tween the stratigraphic ranges of the determined samples. For example, the LAD of Bipedis hannai and Pantanellium sixi is the upper Sinemurian, while the FAD for Gorgansium morganense, Katroma ninstintsi, and Paronaella grahamensis is the lower Pliensbachian. The presence of such contradictions in both of the two most diverse assemblages may be explained by the insuffi- cient current knowledge of the Lower Jurassic radiolarian strati- graphic ranges and occurrences that need more detailed study. The age of this assemblage can be estimated only with caution as a broad range – Sinemurian to Pliensbachian. We cannot currently give a more precise age, but the presen ce of Lower Jurassic radiolarian chert layers in this breccia repre- sents a significant discovery for the stratigraphy of the Dhiarizos Group, as previously a large hiatus (the Lower Jurassic and part of the Middle Jurassic) had been recorded in the typical sections of the Mamonia Complex (BRAGIN & KRYLOV, 1996, 1999). It should be noted that the Lower Jurassic radiolarian cherts are relatively rare in the Mediterranean area (BAUMGARTNER et al., 2003; BORTOLOTTI et al., 2003; CHIARI et al., 2013). Similar rare Lower Jurassic cherts are observed as intercalations within ophiolitic breccia in the Old Zod Pass section of the Lesser Caucasus along the Armenian-Azerbaijan border zone (KNIPPER et al., 1987), and as a chert unit (Angelokastron Chert) covered by the Dhimaina and Potami formations (ophiolitic sandstones and breccias) at the Argolis in Greece (CHIARI et al., 2013). The Lower Jurassic cherts intercalated with micritic limestones were described and dated by TEKIN et al. (2020) in southeastern Turkey. 6. THE ORIGIN AND SIGNIFICANCE OF BRECCIA The studied block of volcaniclastic breccia represents a new un- described unit of the Dhiarizos Group. It differs from other units of the Dhiarizos Group by its composition and origin. The brec- cia consists of fragments of metabasalts, diabases and metagab- bro with minor fragments of siltstones. The supporting matrix of the breccia can vary – from sandy consisting of grains of diabase and other igneous rocks to recrystallized micritic carbonates. Several beds of micritic limestone and radiolarian chert are pre- sent within the breccia. The presence of siltstone fragments and sedimentary contacts between the breccia, limestone and chert beds are an indication of the sedimentary origin of the breccia. The volcaniclastic breccia is closely related with the volcanic units of the Dhiarizos Group, such as the Phasoula and Loutra tis Aphroditis formations, which could be the source of the clastic material. The breccia may have originated via underwater ero- sion of previously formed basic volcanics. The breccia is charac- terized by the irregular, poorly rounded character of the rock G eologia C roatica 125Bragin et al.: The radiolarian age and petrographic composition of a block of the Lower Jurassic volcaniclastic breccia and chert of the Mamonia ... fragments, and by the absence of any sorting or stratification. The deposition of the breccia was probably local – along steep slopes or in narrow depressions triggered by tectonic movements. The formation of the breccia took place simultaneously with deep- water carbonate-chert sedimentation. The beds of micritic lime- stone and radiolarian chert within the breccia display a close af- finity with the Upper Triassic – Lower Jurassic Kholetria Member of the Dhiarizos Group. Similar Mesozoic volcaniclastic sedimentary breccias are known in various regions of the Mediterranean, either related to the upper part of plutonic and intrusive sequences of ophiolite complexes or formed within volcanic sequences (KNIPPER, 1978). The latter type is characterized by the predominance of clastic material consisting of dolerites, basalts and altered gab- bro, while serpentinites are rare. These breccias can occur within or at the top of volcanic sections and they usually have sedimen- tary relationships with chert layers. Such breccias were studied in detail in the Ligurian Alps (GIANELLI & PRINCIPI, 1974). Thus, the Lower Jurassic breccia in the Akamas Peninsula represents the lower part of the Dhiarizos Group sedimentary section. The presence of radiolarian cherts related with volcani- clastic breccia is of significant interest as according to many studi es the Rhaetian to Toarcian (Liassic) cherts are very rare in the Mediterranean Region, and, if present, they can be related to breccias, as in the Lesser Caucasus (KNIPPER et al., 1987) and Greece (CHIARI et al., 2013). 7. CONCLUSIONS Volcaniclastic breccia of sedimentary origin, composed mainly of blocks and clasts of metabasalts, diabase and metagabbro, has been described from the Akamas Peninsula, western Cyprus. Interbeds of radiolarian cherts within breccia yield radiolari an assemblages that allow dating of the breccia as Lower Jurassic, Sinemurian – Pliensbachian. The Triassic volcanics of the Phasoula Formation can be the source of the clastic material of the breccia. The breccia represents a previously unknown lower part of the sedimentary cover of the Triassic volcanics (Phasoula Forma- tion, Mamonia Complex). ACKNOWLEDGEMENTS This work was supported by the Russian Foundation for Basic Research, grant 19-55-25001-Cyprus_a, by the Research and In- novation Foundation of Cyprus (RIF) under the grant Bilateral/ Russia (RFBR)/1118/0025 and by Russian Governmental Assign- ment project 0114-2021-0003. The authors highly appreciate com- ments and corrections suggested by Špela Goričan and Duje Kukoč. 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(1997): Faunal change of Early-Middle Jurassic radiolarians. – News of Osaka Micropaleontologists, Spec. Vol. 10, 155–182. YEH, K.-Y. (1987): Taxonomic studies of Lower Jurassic Radiolaria from east-central Oregon.– National Museum of Natural Science, Special Publication 2, 1–169. YEH K.-Y. (2009): A Middle Jurassic radiolarian fauna from Southfork member of Snow- shoe Formation, east-Central Oregon.– Collection and Research 22, 15–125. YEH, K.-Y. & CHENG, Y.-N. (1998): Radiolarians from the Lower Jurassic of the Bu- suanga Island, Philippines.– Bull. Nat. Mus. Nat. Sci. (Taiwan) 11, 1–65. G eologia C roatica 127Bragin et al.: The radiolarian age and petrographic composition of a block of the Lower Jurassic volcaniclastic breccia and chert of the Mamonia ... Plate 1. Lower Jurassic Radiolaria (Spumellaria) A, B – Pantanellium sixi WHALEN & CARTER; C, D – Gorgansium gongyloideum KISHIDA & HISADA; E – Gorgansium morganense PESSAGNO & BLOME; F – Charlottea weedensis WHALEN & CARTER; G – Paronaella grahamensis CARTER; H – Praehexasaturnalis tetraradiatus KOZUR & MOSTLER; I – Beatricea? argescens (CORDEY); J – Paronaella sp. cf. P. notabilis WHALEN & CARTER; K – Udalia primaeva WHALEN & CARTER; L, M – Udalia spp. Magnification – 1-5, 8 – 1; 6, 7, 9-13 – 2. Scale 100 μm. Figs. A, B, C, G, I, K, L, M – sample 18-15-6; figs. D, E, F, H, J – sample 18-16-7 G eo lo gi a C ro at ic a 128 Geologia Croatica 75/1 Plate 2. Lower Jurassic Radiolaria (Nassellaria) A, B – Bipedis japonicus HORI; C, H – Bipedis hannai WHALEN & CARTER; D – Pseudoeucyrtis busuangaensis (YEH & CHENG); E – Pseudoeucyrtis sp. cf. P. busuangaensis (YEH & CHENG); F, G – Katroma ninstintsi CARTER; I – Bagotum maudense PESSAGNO & WHALEN; J – Canoptum? megathelus CORDEY; K, L – Canoptum sp. cf. C. anulatum PESSAGNO & POISSON; M – Katroma sp. cf. K. irvingi WHALEN & CARTER; N – Lantus sp. cf. L. obesus (YEH). Scale 100 μm. Figs. A, B, F, I, K, L, N – sample 18-15-6, fig. E – sample 18-15-8; figs. C, D, G, H, J, M – sample 18-16-7