ORIGINAL ARTICLES Ordovician–Carboniferous Palynology of El

Home , Ancyrospora, Angochitina, Conochitina

677 Journal of Applied Sciences Research, 9(1): 677-691, 2013 ISSN 1819-544X This is a refereed journal and all articles are professionally screened and reviewed

ORIGINAL ARTICLES

Ordovician–Carboniferous Palynology Of El-Waha-1 Borehole, Western Desert, Egypt.

1Moustafa, T.F, 1Gamal M.A. Lashin and 2Hosny A.M.

1Egyptian Petroleum Research institute, Egypt. 1Botany Department, Faculty of Sciences, Zagazig University, Egypt. 2Geology Department, Faculty of Sciences, El -Azhar University, Egypt.

ABSTRACT

Diverse acritarchs, chitinozoa, and miospore assemblages were recovered from the Palaeozoic sequence in El-Waha -1 well, north western part of the Western Desert. These assemblages forms have many previously described and well known from the Palaeozoic strata in north Gondwana and other parts in the world. The study revealed that the sedimentation was repeatedly interrupted , as is confirmed by stratigraphic breaks. It revealed also that the Ordovician assemblage as well as the lower part of the Silurian are composed mainly of acritarchs and less chitinozoans. No miospors have been recorded. The real sporomorphs are recorded only at the upper part of the Silurian with smooth spores (Retusotriletes, Ambietisporites, Archaeozonotriletes), verrucates ones, and Emphanisporites with porrly defined ribs. The Early Devonian is characterized by zonate – camerate, pseudosaccate, a relatively simple spore types and verrucate ones, that is beside a considerable increase in diversity of the phytoplanktons. The Middle Devonian shows the first incoming of small sculptured camerate spores with thick exoexine and large spinate forms related to genera Hystrichospora, Grandisporites and Ancyrosporites . The Early Carboniferous is dominated by vascular plant taxa including laevigate, cingulizonate and cavate forms. No saccate pollen have been recorded in the studied interval.

Key wrods: Ordovician; Carboniferous; Palynology; El-Waha-1; Western Desert; Egypt.

Introduction

Whilst the Mesozoic and Cenozoic rocks of Egypt have been studied in detail because of their economic significance, the Palaeozoic rocks have received little attention and therefore, the least understood sequence in the area. These rocks have sporadic faunal assemblage which are not useful in age dating , that is why palynology became urgent useful in dating and solving the correlation problem for this part of the Western Desert. The earlier palynological studies in Egypt have been initiated on the Gulf of Suez and Sinai and have concentrated in the Carboniferous rocks. In the Western Desert, only few previous works on the subsurface Palaeozoic palynology were carried out. The work of Gueinn & Rasul (1986) may consider the most extensive one. They established 15 biozones based on palynomorph assemblage ranging in age from Middle Cambrian to Early Permian. Schrank (1987) identified three assemblages belonging to Silurian, Givetian and Visean from Foram -1 well. El-Shamma et al., (1996) recognized five broad-based palynological units ranging in age from Early Visean to Early Permian in two wells (NWD- 302-1 and Faghur-1) located in the north Western Desert. El- Shamma et al., (1998) established 10 assemblage zones ranging in age from the Lower Devonian to the lowermost Carboniferous from three wells in the Western Desert. The present study may consider a continuous trial to shed light about the palynological characteristics of this mistrial succession through the data available from El-Waha-1 well located at the longitude 25º 40\ 09\\ E and latitude 30º 33\ 56 N\\ in the north western part of the Western Desert, this borehole was drilled by Epedeco Sallum company in 1998,

Material and stratigraphic outline:

The regional distribution of the Palaeozoic strata in Egypt shows that there is a thick sequeuce of strata in north west Egypt and a thinner sequeuce in the Gulf of Suez, Sinai area and south west Egypt. Until recently, the Palaeozoic strata of southwest Egypt were undifferentiated due to insufficient stratigraphical evidence. The Ordovician strata are identified in Karkor Talh in the northeastern part of Gebel Oweinat and the Egyptian – Sudan border. This consists of shallow marine sandstone directly above Precambrian basement (Klitzch & Lejal – Nicol, 1984). It is unconformably overlain by sandstone of Silurian age. The Silurian is reported from the subsurface of the north Western Desert by (Schrank, 1984) and ( El-Shamma et al, 2003 ). As

Corresponding Author: Gamal M. A. Lashin, Botany Department, Faculty of Science, Zagazig University, Egypt.

678 J. Appl. Sci. Res., 9(1): 677-691, 2013 in Ordovician time, Egypt was during the Silurian near the eastern edge of the sea which covered a large area of north Africa and reached its maximum extension during Llandovery time. This sea seems to have transgressed into the south west, west and northwest Egypt. Devonian subsurface strata in northwest Egypt were recorded by Schrank (1984) and El-Shamma et al.(1998) through the palynological works. The environment is at least partly marine with a southward increase of continental influence. The Devonian sediments of western Abu Ras Plateau and of northeast Gebel Oweinat are compared with the Tadrat Sandstone Formation of Libya. It's certainly a fluviatile sediment deposited in the southern and eastern to southeastern forland of one (or several) Devonian transgressions. The Carboniferous sediment strata of Egypt differ in facies, and range from fully marine carbonate , shale and deep marine clastics, deltaic and continental fluviatile sandstone to lacustrine and fluvio- glacial deposits. This may due to the structural development of that time. Until late Visean or Namurian, Egypt was at the southern edge of a more or less shallow sea which transgressed parts of the country (klitzch & Léjal – Nicol 1984). At the same time northward draining rivers from surrounding areas in the south and southeast filled depressions with fluviatile sediments. The most applicable lithostratigraphic subdivision for the Palaeozoic sequence in the Western Desert we use here is that adopted by Palaeoservices (1986). This classification seems to be acceptable by Egyptian General Petroleum Corporation (EGPC) and oil companies and includes two formal lithostratigraphical groups. They can also be readily subdivided into formations on the basis of gross lithology A- Siwa Group (early Mid Cambrian – Late Silurian) 1- Shifah Formation (Mid. Cambrian – Mid . Ordovician) 2- Kohla Formation (Late Llandoverian - Ludlovian) 3- Basur Formation (Mid – Late Ludlovian) B- Faghur Group (Early Devonian – Early Permian) 1- Zeitun Formation (Gedinnian – Late Devonian) 2- Desouqy Formation (Tournaisian – Visean) 3- Dhiffah Formation (Late Visean – Late Namurian) 4- Safi Formation (Late Namurian – Early Permian) 112 Ditch samples were obtained from El-Waha-1 well located in the northwestern part of the Western Desert. The samples cover the sequence spanning time interval from the Ordovician to Carboniferous (fig- 1 ) the samples have been subjected to the standard technique of preparation using HF,H Cl and Zn I2 as a heavy liquid separation.

Palynostratigraphy:

Palynomorphs taxa include (acritarchs, chitinozoan and miospores) have been recorded from all samples. This preliminary investigation of the palynomorph assemblages provide a fairly good indication of age since they include many previously described forms known from the Palaeozoic sediments in different parts of the world. The occurrence of the taxa in the studied samples and their stratigraphic range were plotted in figs., 2, 3 and 4.

Ordovician (interval from 3970 to 3765 m):

No sporomorphs have been recorded within this stratigraphic interval. The recovered assemblage is composed mainly of acritarchs and less chitinozoans. Acritarchs, although they are regularly represented between 3955-3845m they are not diverse. The main species here are Visbyosphaeridium subglobosum , Veryhachium sp., Ordovicidinium sp., Timafeevia lancarea , Solisphaeridium sp. and Actinotidiscus crassus. Chitinozoa are represented by Plectochitina sylvanica and Belenochitina sp. The upper lithologic interval between 3845 -3765m is barren. The published acritarchs data for the Ordovician are still somewhat sparse and for this reason, there are several difficulties to establish the real stratigraphic significance of the taxa recorded with exception of very diagnostic species for which the biostratigraphy seems to be known with certitude. No previously data were registered about the Ordovician phytoplanktons in Egypt, and neither Early or Middle Ordovician chitinozoan assemblage has been identified in Libya (Molyneux & Paris, 1985). The Late Ordovician acritarchs which have been identified by these authors are dominated by Veryhachium spp. with Navifusa similis, Ordovicidinium heteromorphicum, Actinotidiscus cf. crassus , Leiofusa sp. and Eupoikilfusa striata. The main chitinozoa which were reported include Armerochitina nigerica, Plectochitina sylvanica, Ancyrochitina merga, Belenochitina capilata and Spinochitina sp.

679 J. Appl. Sci. Res., 9(1): 677-691, 2013

Fig. 1: Location map and stratigraphic log of EL-Waha-1 well.

The Late Caradoc and Ashgill acritarchs which have been reported from Saudi Arabia by Jachowiez (1995) comprise Ordovicidinium eleganthum, Veryhachium subglobosum, Actinotidiscus crassus and Baltisphaeridium sp.. Almostly this could be match with assemblage of JO-1 Biozone be established by Keegan et al., (1990) from Jordan. The recovered phytoplankton assemblage from the present study could be more or less comparable with those data and be referred to the same age (Late Ordovician). The diversification in species taxa, as well as long ranging interval of some of them and lithofacies control make the determination of the precise age for the studied interval is difficult process.

Silurian (interval from 3765 to 3200 m):

This thick stratigraphic succession with its different lithology shows extremely variation in its palynological content. The lower interval between 3765-3710m., has only few chitinozoa species represented by Conochitina inflate and Ancyrochitina sp.. The interval between 3710 – 3560m is barren from any palynomorphs, meanwhile the interval between 3560 – 3440m. is rich with acritarchs and sporadic occurrence of Ancyrochitina sp.. The most represented acritarchs herein are Micrysphaeridium sp., Eupoikolifusa striatifera, Visbyosphaeridium subglobosum, Baltisphaeridium sp., Veryhachium lairdi, V. trispinosum, Diexallophasis remota, D.denticulatus, Polydrixium carnatum and Onondagella deunfi.

680 J. Appl. Sci. Res., 9(1): 677-691, 2013

Fig. 2: Stratigraphic distribution of the Ordovician-Silurian palynomorphs in El-Waha-1 well.

Fig. 3: Stratigraphic distribution of the Devonian palynomorphs in El-Waha-1 well.

681 J. Appl. Sci. Res., 9(1): 677-691, 2013

Fig. 3 Continuo: Stratigraphic distribution of the Devonian palynomorphs in El-Waha-1 well

Fig. 4: Stratigraphic distribution of the Carboniferous miospores in El-Waha-1 well.

682 J. Appl. Sci. Res., 9(1): 677-691, 2013

Chitinozoa are relatively increase upward and represented mainly by Eisenachitina sp., Ancyrochitina ancyrea and Fungochitina pilosa. At sample 3440 m and up; spores show their first record and represented by Retusotriletes goensis, R.aviatus, Archaeozonotriletes chulus, Ambietisporites dilutes, Synorisporites verrucosus, and Emphanisporites neglectus. Many of these taxa have not been recorded in rocks younger than the Upper Silurian sequence elsewhere. This palynomorph assemblage is closely compretable with that reported by El-Shamma et al., (2003) from the Llandoverian strata of NWD-302-1 well in the Western Desert, Egypt A similar assemblage has been also recorded by Gueinn and Rasul (1986) from Llandoveriam- Ludlovian age zone WD-5 of Egypt and by Richardson & Ioannides (1973) from Tanezzoft and Accacus formations of Libya. The record shows somewhat earlier occurrence of verrucate spores (Synorisporites) and Emphanisporites with poorly defined ribs (E.neglectus, E.micrornatus) which present in strata of probably early-middle Ludlovian age. Emphanisporites rotatus and apiculate retusoid spores only occur near the top of the Libyan section. Asimilar spore assemblage has been reported by Richardson & McGregor (1986) within the “Synorisporites tripapillatus – Apiculiretusispora specula” assemblae zone of Downtonian age of the Old Red Sandstone Continent and adjacent regions. An acritarch assemblage with Veryhachium trispinosum, Diexallophasis caperoradiola, Visbysphaeridium sp. and Cymbosphaeridium sp. with chitinozoa of Sphaerochitina sp., Angochitina sp, Conochitina adjelensis, Cyathochitina sp. and spores of Archaeozonotriletes cf. chulus, Ambietisporites dilutes and Dyadospora spp. were reported from the Silurian of Libya by Molyneux & Paris (1985) Onondagella deunfi has a known age spaning the Silurian to Early Devonian in north Africa, that is beside Archaeozonotriletes spp. and Emphanisporites spp. Jardine et al. (1974) and Spina & Vecoli (2009) It is worth to mention that there are some difficulties in using acritarchs for interregional correlation since the geographic distribution of them is considerably influenced by local environmental factors. From the foregoing discussion, we can’t conclude a precise age for the lower part of the studied interval depending on their phytoplankton content, mean while the upper part which bear spores and regular occurrence of acritarchs could be refered to Late Silurian ( Llandoverian -Ludlovian).

Siegenian-Early Emsian (interval from 3200 to 2855 m):

The preliminary palynological investigation of this stratigraphic succession could be subdivided into two assemblages. The first one is recorded between interval 3200 – 2930m. and characterized by spores Calyptosporites sp., Synorisporites verrucosus , Dictyotriletes sp., Ambietisporites sp., Brockotriletes hudsonii and a variety species of genus Emphanisporites (E.rotatus , E.erruticus , E.neglectus , E.spinaeformis and E.obscurus). The upper assemblage between 2930–2855 m. shows the first occurrence of Rhabdosporites langi, Apiculiretusisporites brandti, Verrucosisporites permnus, V. eifeliensis and Emphanisporites annulatus. That is beside most of the prementioned taxa from the lower assemblage Acritarchs show a regular occurrence and represented mainly by Micrysphaeridium stellatum, Gorgonisphaeridium sp., Diexallophasis remota, Polyedryxium carnatun Veryhachium downei, V.trispinosum, Trigulina alargada, Cymatiosphaeridium perimembrana, S.pilaris, Onondagella asymmetrica and Baltisphaeridium sp. Chitinzoan species are relatively few and mostly represented by Ancyrochitina desma, A. ancyrea, A. cornigera, A. tumida, A. longispinosa, Fungochitina pilosa, Lagenochitina sp., Angochitina sp. and Conochitina inculta.

The recovered assemblage in general is demonstrated by many species known to range from the upper part of the Early Devonian into the Middle Devonian and occasionally occur in even younger strata. Furthmore, zonate-camerate spores (Camptozonotriletes) have not been reported from well-dated strata older than Siegenian. Dibolisporites eifeliensis first occurs in Siegenian rocks but only become abundant in the Emsian. El- Shamma et al., (1998) reported Verrucosisporites polygonalis –Dictyotriletes emsiensis Assemblage Zone for the Siegenian of the Western Desert, Egypt. They assigned Emphanisporites annulatus – Camarozonotriletes sextantii Assemblage Zone to the Emsian. Absence of real Emsian taxa such as Grandispora velata, G.nettersheimensis, G.douglastownense, G.mamillata and Ancyrospora acutispinosa indicate that the age may be referred to early Emsian. McGregor & Camfield (1976) indicated that Verrucosisporites polygonalis and Dictyotriletes emsiensis are represented among a typical Upper Siegenian- Lower Emsain assemblage in Canada. Mortimer (1967) mentioned that Retusotriletes, Apiculiretusisporites and Emphanisporites with not developed ribs (Emphanisporites rotatus and E.neglectus) are the most genera in the Siegenian of southern Britain. Massa & Moreau-Benoit (1976) reported Dictyotriletes emsiensis, Dibolisporites eifeliensis, Brochotriletes sp., Emphanisporites spinaeformis and Aurorospora micromanifestus, with

683 J. Appl. Sci. Res., 9(1): 677-691, 2013 chitinozoan Angochitina devonica, Ancyrochitina langi, and A. ancyrea of late Siegenian-early Emsian age of Libya. Richardson et al., (1981) mentioned some facts about the Emsian spores; (1) Dibolisporites eifeliensis has not been recorded before the Lower and Middle Emsian. (2) Emphanisporites erruticus is unknown before the top of the Lower Emsian. (3) Ancyrosporites and Hystrichosporites are absent in the lower part. They do not occur before Upper Emsian together with pseudosaccates and zonate spores in the upper most Emsian. Riegel (1974&1982) mentioned too that spores of Ancyrosporites nettershiemensis and Hystrichosporites microancyreus occur first at about mid-late Emsian age. The same conclusion has been mentioned by Streel et al., (1975) from the Denant Basin. Emphanisporites annulutus begins in south west Eifel in the lower part of Upper Emsian (Lanninger, 1968) and at probably Middle Emsian at Gaspe Bay (McGregor, 1973) and probably Emsian (Streel et al., 1975). McGregor (1973) concluded that the specimens of Grandisporites dauglastwense, G.macrotuberculata and Dibolisporites echinaceus appear at the middle of Upper Emsian. In this respect, it seems appropriate to note that the Siegenian/Emsian boundary may occur in the present interval but it is difficult to locate it. Position of the boundary itself has not been defined, since no obvious changes in composition of the spore assemblage could be detected through the present interval. This interval is thus included in an undifferentiated palynostratigraphic unit of Siegenian/Emsian time.

Eifelian (interval from 2855 to 2630 m):

The recovered assemblage from this stratigraphic interval shows an extinction of some characteristic Emsian spores such as Rhabdosporites langi, Brochotriletes hudsonii and Apiculiretusisporites brandti ; other new characteristic forms show their first incoming such as; Grandisporites douglastwense, G.nettershemensis, G.libyensis, Spinozonotriletes naumovi, S.langi, hystrichosporites bifurcata, H.gravis, H.longispinosa and Hymenozonotriletes discoris. Marine chitinozoan and acritarchs still persisting and represented by most of the Emsian taxa although they are less abundant. The recorded assemblage is characterized by a proliferation of the large apiculate and spinose, zonate-pseudosaccate spores (Grandispora, Hymenozonotriletes, Rhabdosporites and Spinozonotriletes). All of these are typical Middle Devonian taxa. El-Shamma et al. (1998) reported that the Eifelian palynomorphs of Faghur-1 and NWD-302-1 wells, Western Desert are characterized by occurrence of Hymenozonotriletes discors, Grandispora inculta, G.velata, Veryhachium trispinosum, Diexallophasis caperoradiata, Fungochitina pilosa, Angochitina devonica, Ancyrochitina tumida, A.desma and Alpenachitina cornigera. An assemblage with Hystrichosportites spp., Grandisporites libyensis and Ancyrosporites nettershemensis has been reported from Eifelian sediments by Massa & Moreau-Benoit (1976), Paris et at., (1985) from Libya. This is closely comparable with those recorded by Jardine’ & Yapaudjian (1968) from Algeria, and by Hemer & Nygreen (1966) from Saudi Arabia. Loboziak & Streel (1995) recorded an assemblage with Grandispora riegeli, Emphanisporites annulatus, Acinosporites lindlarensis, Verrucosisporites premnus and V.scurrus. The Saudi assemblage was recorded from beds of uncertain age but it thought to be of Eifelian age based apparently on its stratigraphic position. The recovered assemblage here could be also related to zone “G.douglatowense – A.eurypterata” of Richardson & McGregor (1986) of Eifelian age. It should be mention here, that the data available for comparison indicated that the Eifelian assemblage of the present study has more in common with those from the north African region rather than those from elsewhere. Givetian (interval from 2630 to 2555 m) An abrupt change both in the quantity and diversity of taxa has been recorded within this interval. Most of the previously recorded taxa have been distincted. The main represented spores herein are Retusosporites spp., Grandisporites inculta, Ancyrosporites acutispinosa, Geminospora lemurata and Hystricosporites gravis. Marine acritarchs and chitinozoans are represented sporadically with few long-ranging forms related to genera Veryhachium, Polydryxium, Dixallophasis, Fungochitina and Conochitina. The first occurrence of small sculptured camerate spores with a thick exoexine such as Geminospora lemurata and its related species is regarded as the most spore marker to locate the base of the Givetian stage (Streel & Loboziak, 1994). Most-if not all –of these recovered taxa were reported by El Shamma et al. (1998) from Faghur-1 and NWD-302-1 wells in the Western Desert, of Egypt and assigned to the Givetian age. The recovered assemblage carries also the general characteristic features of the Givetian microflora encountered in Libya by Paris et al. (1985) and Mossa & Moreau-Benoit (1976)., Streel et al., (1988) , Loboziak & Streel (1989) and Grignani et al., (1992).

684 J. Appl. Sci. Res., 9(1): 677-691, 2013

A corresponding Givetian spores assemblages “Densosporites devonicus –Grandisporites naumovi” and “Geminospora lemurata-Cymbosporites manificus” zones suggested by Richardson & McGregor (1960) are rich with Grandispora, Ancyrospora, Rhabdosporites and Aneurospora. Other data available from many localities of the world indicates that the Givetian assemblage of the Egyptian Western Desert is generally similar to those recorded from the Old Red Sandstone continent and adjacent regions (Richardson & McGregor, 1986), Poland (Turnau, 1986, 1996), Shetland (Marshall & Allen, 1982), Canada (McGregor & Camfield, 1976, 1982), from the Parana Basin; BBrazil (Loboziak et al., 1988 and Loboziak and Melo, 2000).

PLATE I

PLATE I Fig. 1: Rhabdosporites minutes (Balme) Playford. Fig. 2: Cymbosporites proteus McGregor & Camfield. Fig. 3: Stenozonotriletes simplex Naumova Fig. 4: Punctatisporites Punctatus Ibrahim. Fig. 5: Retusotriletes goensis Lele & Streel. Fig. 6: Synorisporites verrucatus Richardson & Ioannides Fig, 7: Archaeozonotriletes sp. Fig. 8: Aneurospora sp. Fig. 9: Dibolisporites sp. Fig. 10: Retusotriletes cf. communis Naumova Fig. 11: Dibolisporites eiflelinsis (Lanninger) McGregor Fig. 12: Syynorisporites Lybicus. Richardson & Ioannides Fig. 13: Apiculiretusisporites plicata (Allen) Streel. Fig. 14: Craspedispora sp. Fig. 15: Brockotriletes sp. Figs. 16: 22: Emphanisporites rotatus McGregor. Fig. 17: Emmphanisporites erruticus Eisenaek. Figs. 18: 19: Dictyotriletes emsiensis (Allen) McGregor. 685 J. Appl. Sci. Res., 9(1): 677-691, 2013

Fig. 20: Emphanisporites sp Fig. 21: Emphanisporites annulatus McGregor. Figs. 23, 24: Emphanisporites spinaeformis Schultz. Fig. 25: Emphanisporites abscurus McGregor Fig. 26: Verrucosisporites scurrus (Naumova) McGregor & Camfield Fig. 27: Lophozonotriletes sp.

PLATE II

PLATE II Fig. 1: Brockotriletes hudsonii McGregor & Camfield. Fig. 2: Dictyotriletes emsiensis (Allen) McGregor. Fig. 3: Endosporites micromanifestus Hacquebard. Fig. 4: Hymenozonotriletes discors Chibrickova. Fig. 5: Comptozonotiletes caperatus McGregor Fig. 6: Spelaeotriletes cf crustatus Higgs Fig, 7: Geminospora lemurata (Balme) Playford. Fig. 8: Verrucosisporites polygonalis Lanninger. Fig. 9: Apiculiretusisporites brandti Streel. Fig. 10: Grandispora protea (Naumova) Moreau Benoit Fig. 11: Ancyrospora acutispinosa Chi & Hills. Fig. 12: Ancyrospora longispinosa Richardson Fig. 13: Grandisporites libyensis Moreau Benoit Fig, 14: Grandispora inculta Allen Fig. 15: Camarozonotriletes sp. Fig. 16: Diatomozonotriletes sp. Fig. 17: Synoriporites papillensis McGregor Fig. 18: Verrucusisporites premnus Richardson

686 J. Appl. Sci. Res., 9(1): 677-691, 2013

Fig. 19: Aratrisporites sahariensis Loboziak & Alpern. Fig. 20: Rugospora flexuosa (Jushko) Streel Fig, 21: Dipolisporites echinaceus (Eisenack) Richardson. Fig, 22: Verrucosisporites nitidus (Naumova) Playford

PLATE III

Fig. 1: Spelaeotriletes owensi Loboziak & Alpern. Fig. 2: Vallatisporites agadesi Loboziak & Alpern. Fig. 3: Spelaeotriletes triangulus Neves & Owens Fig. 4: Radiizonates genuinus Loboziak & Alpern. Fig. 5: Vallatisporites pusillites (kedo) Dolby & Neves Fig. 6: Vallatisporites verrucosus Playford. Fig, 7: Spelaeotriletes bengahaziensis Loboziak & Alpern. Fig. 8: Spelaeotriletes arenuceus Neves & Owens Fig. 9: Umbonatisporites sp. Fig. 10: Retusotriletes crassus Clayton, Johnston, Sevastogolo & Smith Fig. 11: Vallatisporits ciliaris (Luber) Sullivan. Fig. 12: Spore type A Clayton &Loboziak Fig. 13: Convulatisporites cf. mellita Hoffmeister, Staplin & Malloy

687 J. Appl. Sci. Res., 9(1): 677-691, 2013

PLATE IV

Fig. 1: Veryhachium lairdi Cramer. Figs. 2, 11: Micrhysphaeridium stellatum Deflandre. Figs. 3, 12: Ononadagella asymmetrica (Deunff) Cramer. Figs. 4, 10, 15, 16: Baltisphaeridium spp. Fig. 5: Diexallophasis caperoradiola Lioblich. Fig. 6: Veryhachium trispinosum (Eisenack) Deunff. Fig, 7: Veryhachium downei Stockmans & Willieri. Fig. 8: Diexallophasis remota (Deunff) Playford. Fig. 9: Triangulina alargada Cramer. Fig. 13: Cymatiosphaera perimembrana Staplin. Fig, 14, 20: Polyedriyxium carnatum Playford. Fig. 17: Navifusa bacillum (Deunff) Playford. Fig. 18: cf. Baltisphaeridium sp Fig.19: Actinotidiscus crassus Loeblich & Tappan. Fig. 21: Cymatiosphaera sp. Fig. 22: Timofeevia lancarae (Cramer & Diez) Vanguestaine

688 J. Appl. Sci. Res., 9(1): 677-691, 2013

PLATE V

Fig. 1: Ancyrochitina sp. Fig. 2: Ancyrochitina tumida Taugourdeau & Jekhowsky. Fig. 3, 9: Ancyrochitina cornigera Collinson & Scott. Fig. 4: Angochitina cullinsoni Taugourdeau & Jekhowsky. Fig. 5: Ancyrochitina spinosa Eisenack. Fig. 6: Ancyrochitina capillata Eisenack. Figs, 7, 8: Ancyrochitina ancyrea Eisenack. Figs. 10, 11: Angochitina devonica Eisenack. Fig. 12: Fungochitina pilosa Collinson & Scott. Fig. 13: Desmochitina sp Fig, 14: Ancyrochitina desmea Eisenack. Figs. 15, 19: Belenochitina sp. Fig. 16: Angochitnia sp. Fig. 17: Conochitina sp. Fig. 18: Desmochitina aranea Urban. Fig. 20: Conochitina inflate Wood.

689 J. Appl. Sci. Res., 9(1): 677-691, 2013

Carboniferous:

Visean (interval 2555-2230m) The dominant fraction of the organie matter of this stratigraphic interval is of continental origin. Miospores are abundant , most of them belong to smooth (Retusotriletes), apiculate (Apiculiretusitriletes) to verrucate (Verrucosisporites) as well as to a variety of genera Densosporites, Radiizonotes and Vallatisporites . The palynological association of this stratigraphic interval could be subdivided into two interfered assemblages , both is related to the Visean age since they have many shared taxa , at the same time some different playnological events are observed Early Visean (interval 2555-2335 m) The assemblage recorded herein is characterized by some important taxa include ; Lycospora pusilla, Densosporites annulatus, D. spiniferites, Vallatisporites vallatus, V.verrucosus, V. nitidus, Raistrickia spatulata, Spelaeotriletes arenaceous, S.balteatus, Diatomozonotrites fragilis, Radiizonates genuinus, Convulatisporites mellita, Aratrisporites sahariensis. that is besides other spores belonging to genera Punctatisporites. Calamaspora, Retusotriletes, Granulatisporites and Umbonatisporites. Most, if not all, these microfossils were recorded from the Lower Visean sediment of NWD – 301-1 well by El-Shamma et al. (1996) and included in WD-13 zone which was suggested by Gueinn & Rasul (1986). The assemblage has shared species with zone (II) of Visean age assigned by Kora & Schultz (1987) Um Bogma, Sinai such as Punctatisporites spp., Retusotrilete sp., Verrucosisporites sp., Convulatisporites sp., and Calamaspora sp. and with zone (A) of Visean from central Sinai by Kora (1993). Asimilar assemblage of early Visean age has been noted by Clayton and Loboziak (1985), and Loboziak & Clayton (1988) ,from north east Libya , Grignani et al., (1992) from Al-Kufra Basin of south east Libya , Attar et al., (1980) in Algeria , Loboziak et al., (1991) from Brazil , Coquel et al., (1995) from northern Niger , and Melo & Loboziak (2003) from Amazon Basin , northern Brazil.

Late Visean (interval 2335-2230m):

Many taxa from the preceding age are common elements herein particularly; Aratrisporites, sahariensis, Lycospora pusilla, Vallatisporites vallatus, Verrucosisporites nitidus, Radiizonates genuinus and Diatomozonotrileter fragilis. Other species have their real occurrence in this stratigraphic interval such as ; Spelaeotriletes triangulus , S. owensi, Vallatisporites agadesi, V. ciliaris, Raistrickia clavata and R.spatulata Sultan (1986) established Zone-I from Wadi Araba with spores Punctatisporites sp. Raistrickia sp., Densosporites sp. and Convulatisporites sp. which are dated as Late Visean , the same association has recovered also by Schrank (1984), Kora & Schultz (1987) , El-Shamma et al., (1996) in Egypt. In north Africa , the frist occurrence of Lycospora pusilla was considered by Massa et al., (1980), Loboziak& Cloyton (1988) and Coquel & Massa (1993) to occur only in Late Visean. The recovered assemblage could be correlated too by those reported by Clayton & Loboziak (1985) in Libya, Attar et al., (1980) from Sahara Algeria , and by Melo & Loboziak (2003) from northern Brazil.

Early Namurian (2230 – 2125 m):

The miospores recovered within this stratigraphic interval are distinguished by the flourishing of smooth types (Calamaspora, Retusotriletes, Punctatisporites), apiculate (Apiculiretusipora spp.) and cingulicavate forms as Vallatisporites and Spelaeotriletes. The most characterizing taxa represented here are Vallatisporites ciliaris, Spelaeotriletes benghaziensis and S.owensi. That is besides many of Visean forms related to genera Granulatisporites, Convulatisporites, Densosporites, Diatomozonotriletes and Radiizonates. This assemblage is similar to that recorded in WD-13 and WD-14 zones of Gueinn & Rasul (1986) by the presence of Spelaeotriletes owensi, S.arenaceous, Lycospora pusilla and absence of monosaccate pollen. The same conclusion is mentioned by Kora & Schultz (1987) and Sultan (1986). The assemblage is also correlated with miozone (ΙΙΙ) of Early Namurian assigned by El-Shamma et al. (1996) from NWD-302-1, Faghur-1 and west Faghur-1 wells, Western Desert specially in presence of Densosporites spp., Spelaeotrilets triangulus, S.benghaziensis Vallatisporites verrucosus, Diatomozonotriletes fragilis, Vallatisporites agadesii and Calamospora sp. The Serpukhovian age which noted by Massa et al. (1980) from Libya comprises Lycospora pusilla, Vallatisporites ciliaris and Spelaeotriletes triangulus. The same conclusion was mentioned by Clayton & Loboziak (1985) and by Loboziak & Clayton (1988) and from north Niger by Coquel et al. (1995) and referred to early Namurian.

690 J. Appl. Sci. Res., 9(1): 677-691, 2013

Conclusions:

The present study revealed that, the sedimentation in the present borehole was repeteadly intrupted, as inconfermed by stratigraphic breaks between different ages. Some of these breaks are matching with the general structural breaks in the stratigraphy of Egypt and north Africa such as that between the Ordivisian/Silurian, Silurian/Devonian and Devonian/Carboniferous. Other breaks may be cosidered as local stratigraphic ones represented by decreasing in thickness of some ages or their competely absences. The diversication in acritarchs species recorded in many correletable areas, as well as, along ranging intervals of some of them and lithofacies change prevent determination of the precious age of some studied intervals such as the Ordovisian and Silurian. An abrupt change in palynomorph diversity between the Eifelian and Givetian was recorded as indicated by the proliferation of large spinate spores in the Givetian. No saccate pollen have been recorded in the studied Carboniferous interval, at least at the beginning of the Namurian age.

References

Attar, A., J. Fournier, A.M. Candilier, & R. Coquel, 1980. Etude palynologique du Devonien terminal et du Carbonifére inferieur du basin D'illize (Fort–Polignac) Algerie. Rev. Inst. Franc. du Pétrole, 35(4): 585-610. Clayton, G. & S. Loboziak, 1985. Early Carboniferous (Early Viseán–Serpukhovian) palynomorphs, in: Palynostratigraphy of North–East Libya. Jour. Micropalaeontology, 4(1): 83-92. Coquel, R., J. Lang, & M. Yahaya, 1995. Palynologie du Carbonifére du Nord Niger et de la plate–forme saharienne–implications stratigraphiques et paléogéographiques. Rev. Palaeobot. Palynol., 89(3,4) : 319- 334. Coquel, R. & D. Massa, 1993. A propos d' événements palynologiques du Carbonifére inférieur (= Mississipien) d' Afrique du Nord. Ann. Soc. Géol. Nord, 2: 145-152. El–Shamma, A.A., W.M. Abdel Malik, A.A. Baioumi, & T.F. Moustafa, 1996. Microfloral characteristics of some Carboniferous rocks in the Western Desert, Egypt. Bull. Fac. Sci., Assiut Univ., 25(2–F): 107-124. El–Shamma, A.A., T.F. Mostafa, & W.M. Abdel Malik, 1998. Devonian spores from subsurface rocks in the Western Desert, Egypt. Proceedings of the 14th Petroleum Conference, EGPC, Cairo, 1: 451-465. El–Shamma, A.A., A.A. Baioumi & G. Lashin, 2003. Silurain palynomorhs from NWD-302-1 Western Desert, Egypt. Egyptian J. of Paleont., 3: 179-188. Grignani, D., E. Lanzoni, & H. El–Atrash, 1992. Palaeozoic and Mesozoic subsurface palynostratigraphy in the Al–Kufra Basin, Libya. Proceedings of the 3th Symposium on the Geology of Libya (Tripoli, 1987), pp: 1159-1227. Gueinn, K.J. & S.M. Rasul, 1986. A contribution to the biostratigraphy of the Palaeozoic of the Western Desert, utilizing new palynological data from the subsurface. 8th EGPC, Petrol. Conf., Cairo, pp: 1-23. Hemer, D.O & P.W. Nygreen, 1967. Devonian Palynology of Saudi Arabia. Rev. Palaeobot.Pallynol., 5: 51-61. Jachowicz, M., 1995. Ordovician acritarch assemblage from central and northwestern Saudi Arabia. Rev. Palaeobot Palynol., 89: 19-25, this issue. Jardiné, S., A. Combaz, L. Magloire, G. Peniguel, & G. Vachey, 1974. Distribution stratigraphique des Acritarches dans le Paléozoique du Sahara Algérien. Rev. Palaeobot. Palynol., 18(1, 2): 99-129. Jardiné, S. & L. Yapaudjian, 1968. Lithostratigraphie et palynologie du Dévonien–Gothlandien gréseux du Bassin de Polignac (Sahara). Rev. Inst. Franc. du Pétrole, 23: 439–469. Keegan, J.B., S.M. Rasul, & Y. Schaheen, 1990. Palynostratigraphy of the lower Paleozoic,, Cambrian to sulurian of the Hashemite Kingdom of Jordan. Rev. Palaeobot. Palynal., 66: 167-180. Klitzsch, E-& A. Lejal – Nicol, 1984. Flora and Founa from a strata in southern Egypt and north Sudan (Nubai and surrounding area). Berl. Geowiss. Abh., 50(A): 47-79. Kora, M., 1993. Carboniferous miospore assemblages from the Abu Rodeiyium boreholes, west–central Sinai, Egypt. Rev. Micropaléontologie, 36(3): 235-255. Kora, M. & G. Schultz, 1987. Lower Carboniferous palynomorphs from Um Bogma, Sinai, Egypt. Grana, 26: 53-66. Lanninger, E.P., 1968. Sporen–Gesellschaften aus dem Ems der SW–Eifel. Palaeontographica, Abt., B. 122: 95-170. Loboziak, S. & G. Clayton, 1988. The Carboniferous palynostratigraphy of northeast Libya. in: A. El–Arnauti, B. Owens & B. Thusu (eds.), Subsurface Palynostratigraphy of Northeast Libya. Garyounis University Publications, Benghazi–Libya, pp: 129-149. Loboziak, S. and J. Melo, 2000. Middle Devonian-Silurian miospores biostratigraphy in the southwestern outcrop belt of the Purnaibu Basin, North-central Brazil. Rev. of Micropal., 43: 301-318. Loboziak, S. & M. Streel, 1995. Late Lower and Middle Devonian miospores from Saudi Arabia. Rev. Palaeobot. Palynol., 89(1, 2): 105-113. Loboziak, S., M. Streel, & M.I.A. Burjack, 1988. Miospores du Dévonien moyen et supérieur du bassin du Paraná, Brésil: systématique et stratigraphie. Sci. Géol., 41(34): 351-377.

691 J. Appl. Sci. Res., 9(1): 677-691, 2013

Loboziak, S., M. Streel, M.V. Caputo, & J.H.G. Melo, 1991. Evidence of west European defined miospore zones in the uppermost Devonian and Lower Carboniferous of the Amazonas Basin (Brazil). Géobios, 24: 5-11. Loboziak, S. & M. Streel, 1989. Middle–Upper Devonian miospores from the Ghadamis Basin (Tunisia–Libya): Systematic and stratigraphy. Rev. Palaeobot. Palynol., 58: 197-203. Marshall, J.E.A. & K.C. Allen, 1982. Devonian miospore assemblages from Fair Isle, Shetland. Palaeontology, 25(2): 277-312. Massa, D., R. Coquel, S. Loboziak, & J. Taugourdeau–Lantz, 1980. Essai de synthése stratigraphique et palynologique du Carbonifére en Libye occidentale. Ann. Soc. Géol. Nord, 99: 429-442. Massa, D. & A. Moreau–Benoit, 1976. Essai de synthése stratigraphique et palynologique du Systéme Dévonien en Libye occidentale. Rev. Inst. Franc. du Pétrole, 31(2): 287-333. McGregor, D.C., 1973. Lower and Middle Devonian spores of eastern Gaspé, Canada. I: Systematics. Palaeontographica, Abt., B, 142: 1-77. McGregor, D.C. & M. Camfield, 1976. Upper Silurian ? to Middle Devonian spores of the Moose River Basin, Ontario. Geol. Surv. Canada, Bull., 263: 1-63. McGregor, D.C. & M. Camfield, 1982. Middle Devonian miospores from the Cape de Bray, Weatherall, and Helca Bay Formations of northeastern Melville Island, Canadian Arctic. Geol. Surv. Canada, Bull., 348: 1- 105. Melo, S. & S. Loboziak, 2003. Devonian – Early Carboniferous miospore biostratigraphy of the Amazon Basin, Northern Brazil ,Rev. Palaeobot. Palynol., 124: 131-202. Molyneux, S.G. & F. Paris, 1985. Late Ordovician palynomorphs. in: B. Thusu & B. Owens (eds.), Palynostratigraphy of North–East Libya. Jour. Micropalaeontology, 4(1): 11-26. Mortimer, M.G., 1967. Some Lower Devonian microfloras from souther Britain, Rev. Palaeob. Palynol., 1: 95- 109. Palaeoservices Ltd., 1986. The hydrocarbon potential of the Palaeozoic rocks of the Western Desert, Egypt. Non–exclusive EGPC/ Palaeoservices Report, Palaeoservices, Watford, U. K. Paris, F., J.B. Richardson, W. Riegel, M. Streel, & M. Vanguestaine, 1985. Devonian (Emsian–Famennian) palynomorphs. in: B. Thusu & B. Owens (eds.), Palynostratigraphy of North–East Libya. Jour.Micropalaeontology, 4(1): 49-82. Richardson, J.B. & D.C. McGregor, 1986. Silurian and Devonian spore zones of the Old Red Sandstone Continent and adjacent regions. Geol. Surv. Canada, Bull., 364: 1-79. Richardson, J.B. & N. Ioannides, 1973. Silurian palynomorphs from the Tanezzuft and Acacus Formations. Tripolitania, North Africa. Micropalaeontology, 19 (3): 257-307. Richardson, J.B., S.M. Rasul, & T. Al–Ameri, 1981. Acritarchs, miospores and correlation of the Ludlovian– Downtonian and Silurian–Devonian boundaries. Rev. Palaeobot. Palynol., 34(2): 209-224. Riegel, W., 1974. Spore floras across the Lower–Middle Devonian boundary in the Rhineland (G. R. F.). Palynology of the Proterophyte and Palaeophyte, Proc. 3rd Internat. Palynol. Conf., pp: 47-53. Riegel, W., 1982. Palynological aspects of the Lower / Middle Devonian transition in the Eifel region. Courier Forschungsinstitut Senckenberg, 55: 279-292. Schrank, E., 1984. Palaeozoic and Mesozoic palynomorphs from the Foram–1 well, Western Desert, Egypt. N. Jb. Geol. Paläont. Mh., 2: 95-112. Schrank, E., 1987. Palaeozoic and Mesozoic palynomorphs from northeast Africa (Egypt and Sudan) with special refrence to Late Cretaceous pollen and dinoflagellates. Berliner Geowiss. Abh. (A), 75(1): 249-310. Spino, S. & M. Vicoli, 2009. Palynostratigraphy and vegetational changes in the Siluro-Devonian of the Ghadamis Basin , North Africa. Palaeogeography, Palaeoclimatology, Palaeoecology, 282: 1-18. Streel, M., M. Fairon–Demaret, & N. Otazo, 1975. Siegenian and Emsian spores from the Dinant Basin (Belgium). Comm. Internat. Microflore Paléozoique, Newsletter., 10: 7. Streel, M., F. Paris, W. Riegel, & M. Vanguestaine, 1988. Acritarchs, chitinozoan and spore stratigraphy from the Middle and Late Devonian of northeast Libya. in: A. El–Arnauti, B. Owens & B. Thusu (eds.), Subsurface Palynostratigraphy of Northeast Libya. Garyounis University Publications, Benghazi: Libya, pp: 111-128. Streel, M. & S. Loboziak, 1994 a. Observations on the establishment of a Devonian and Lower Carboniferous high–resolution miospore biostratigraphy. Rev. Palaeobot. Palynol., 83: 261-273. Sultan, I.Z., 1986. Palynostratigraphy of Carboniferous rock sequence in Wadi Araba well No. 1, Gulf of Suez region, Egypt. Sci. Géol. Bull. Strasbourg, 39(4): 337-360. Turnau, E., 1986. Lower to Middle Devonian spores from the vicinity of Pionki (central Poland). Rev. Palaeobot. Palynol., 46: 311-354. Turnau, E., 1996. Miospore stratigraphy of Middle Devonian deposits from Western Pomerania. Rev. Palaeobot. Palynol., 93(1–4): 107-125.