preliminary palynological and depositional … · regressive phase, the mamu formation composed of...

International Journal of Geology, Earth & Environmental Sciences ISSN: 2277-2081

An Open Access, Online International Journal Available at http://www.cibtech.org/jgee.htm

2019 Vol. 9 (2) May-August, pp. 1-13/Uzodimma and Adegboyega

Research Article

Centre for Info Bio Technology (CIBTech) 1

PRELIMINARY PALYNOLOGICAL AND DEPOSITIONAL

ENVIRONMENT ASSESSMENT OF THE EZINACHI CLAY

SOUTHEASTERN NIGERIA

*Durugbo Ernest Uzodimma1 and Olayiwola Moshood Adegboyega

2,3

1Department of Biological Sciences, Redeemer’s University, P.M.B. 230, Ede, Osun State, Nigeria

2Natural History Museum, Obafemi Awolowo University, Ile-Ife, Osun State, Nigeria

3Evolutionary Studies Institute (ESI), and School of Geosciences, University of the Witwatersrand,

Johannesburg, South Africa

*Author for Correspondence: [email protected]

ABSTRACT

Depositional environments of sedimentary clay play a significant impact on the industrial applications of

clay. Palynological technique was used to analyze thirteen outcrop samples to reconstruct depositional

environment and assign age to the Ezinachi Kaolinitic Clay Deposit, Southeastern Nigeria for the first

time. The palynological analysis revealed sparse records of pollen and spores especially Ephedripites

multicostatus, Lycopodiumsporites sp., Proteacidites dehaani, Longapertites marginatus, L.

vanendeenburgi, Proxapertites operculatus, P. sulcatus, Retidiporites magdalenensis, Echitriporites

trianguliformis, Cyathidites minor, Leotriletes adriennis, Distaverrusporites simplex, Laevigatosporites

spp., Cicatricosisporites sp., Polypodiaceoisporites sp. and sparse records of the dinoflagellate cysts

Oligosphaeridium complex, Cordosphaeridium inodes, C. fibrospinosum, C. exilimurum, Homotryblium

tenuispinosum, H. abbreviatum, Spiniferites ramosus, Operculodinium centrocarpum, Polysphaeridium

subtile, Lejeunecysta sp., Hystrichokolpoma sp., Achomosphaera sp., Cleistosphaeridium sp., the

acritarch Leiosphaeridia spp., Microforaminiferal wall linings, co-occurring with common fungal

elements, diatom frustules and rare freshwater algae. The common records of structureless organic matter

coupled with moderate structured and degraded phytoclasts suggests sediment deposition in a shallow to

marginal marine environments. The lithostratigraphic unit consists of clayey sands, shales, and claystones

with sand intercalation. The stratigraphic ranges of the recovered palynomorphs suggests a Late

Paleocene – Eocene age for the Ezinachi clay.

Keywords: Palynomorphs, Dinoflagellate cysts, Phytoclasts, Ezinachi Clay, Shallow marine, Marginal

Marine

INTRODUCTION

Though several paleontological studies of the sediments in south eastern Nigeria have been carried out by

different workers (Oboh-Ikuenobe et al., 2005; Edet and Nyong, 1993; Umeji ,2006; Umeji and Nwajide,

2007; Umeji and Edet, 2008; Chiaghanam et al.,2012; Soronnadi-Ononiwu et al., 2012; Durugbo, 2013;

Soronnadi-Ononiwu and Omoboriowo, 2013), from available literature no published record of

paleontological / palynological studies of the Ezinachi clay exists. The few published records on the clay

were aimed at assessing its chemical potentials. Akaranta and Wankasi (1996) had tested samples of the

Ezinachi clay, a kaolin clay as an extender in coatings. They had posited that Nigerian clay minerals have

been studied mostly for mineralogical contents and composition. Njoku et al., (2000), using aqueous

solutions of the clay, had tested its potential as an adsorbent of copper and lead ions. Other workers

include (Okoye and Obi, 2011; Okoye and Otolo, 2012; Okoye, et al., 2012a,b), who applied it as

catalysts for esterification of ethanol and Acetic acid, and later investigated its adsorption kinetics among

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others. The Ezinachi clay factory was established in 1980 by the administration of the first civilian

governor of Imo State, late Chief Sam Onunaka Mbakwe to harness the readily available natural resource

for commercial purposes which involved making of bricks for house construction, manufacturing of

flower vases, plates and dishes. The factory had stopped operation since 1990 and it is presently

overgrown with weeds (Fig. 1).

Palynology has been a very useful tool in the reconstruction of depositional environment of sedimentary

rocks in Nigerian basins. Prominent among these are the works of (Oboh,1992, 1995, Oboh and

Salami,1992) etc. The usage of palynology in the reconstruction of palaeoenvironments of Nigerian clays

and clay minerals has never been reported in literature. However, the Lawrence clay pit, Henry County,

Tennessee, was suggested to be deposited during Middle Eocene in a stagnant body of water by using

palynomorphs assemblage (Dilcher,1973, Elsik and Dilcher,1974). Again, Jolley and Spinner (1989) had

analyzed the London Clay and reported the dinoflagellate cyst suite characterized by common records of

Wetziellia Furthermore, they cited Knox and Harland (1979),who reported the presence of dinoflagellates

in some samples from Harwich Member and recognized the presence of the Apectodinium hyperacanthum

Zone of Costa and Downie (1976). They also recognized and proposed an acme of Deflandrea

oebisfeldensis Alberti 1959 within the upper part of the hyperaeanthum Zone. In addition , they

recognized a unique association composed of Hystrichosphaeridium tubiferum, Glaphyrocysta

ordinate,Lejeunecysta hyaline,Diphyes colligerum, Lentinia wetzelii, Cerodinium wardenense,

Deflandrea denticulata and Adnatosphaeridium multispinosum.

Other techniques that can be used for the understanding depositional environment of clay mineral deposits

include petrographic and granulometric data, sedimentological data, X-ray diffraction, TEM, SEM, EDX,

and chemical analyses (Soman and Machado,1986 ; Ingles and Anadon,1991). The sedimentary clay,

otherwise known as secondary clay, has more environmental and industrial benefit than the residual clay.

The sedimentary clay minerals have various depositional environments (Ingles and Anadon,1991). Some

of these are flood plain, mudflat fresh, organic-rich lakes, sabkha (salt flat), playa-lake and lagoon

palaeoenvironments (Ingles and Anadon,1991). Research has shown that depositional environments have

a large influence on the engineering and geotechnical properties of clays. Stress history, undrained and

drained shear-strength parameters, liquid limit and plastic limit and activity of clay minerals are among

properties that can be affected by their depositional environments (Chung and Finno, 1992;Wu et al.,

2014). Other engineering/geotechnical properties of clays affected by depositional environments are the

consistency limits and activity, the Cu/p value, the over-consolidation ratio values, consolidation

settlement, and artesian pressure (Graham and Shields,1985; Ohtsubo et al., 1995; Chung et al.,

2002,2005; Bo et al., 2015). However, information about the relationships between depositional

environments of clay deposits and engineering/geotechnical properties would be quite helpful to

understand the spatial variation of engineering/geotechnical properties of clay as well as the effect of

sample disturbance (Chung et al., 2004, 2005). Therefore, the aim of this study is to use palynological

data to date and assess the depositional environments of the Ezinachi Clay Southeastern, Nigeria. This is

crucial for better understanding of the depositional history of the Ezinachi clay deposit in order to

enhance its industrial benefits.

Description of study site /Geology of Southeastern Nigeria

Ezinachi town is few kilometers from both Okigwe town and Umuahia the Abia state capital south eastern

Nigeria (Fig. 1). The sedimentary formations around Okigwe southeastern Nigeria have been attributed to

the Anambra Basin (Umeji and Nwajide, 2007; Umeji and Edet, 2008; Ahiarakwem and Onyekuru, 2011;

Durugbo, 2013). Akande and Erdtmann (1998) had described the Anambra Basin as a synclinal structure

composed of more than 5000 m thick sediments spanning the early Cretaceous to Recent which

developed following the third phase of sedimentation in the Benue Trough. Chiaghanam et al., (2012) had




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reported that the Anambra Basin sedimentation commenced in the Campanian with the Nkporo Shale,

Enugu Shale and Owelli sandstones which all made up the Nkporo Group forming the basal beds of the

Campanian period characterized by a short period of marine transgression and regression. During the

regressive phase, the Mamu Formation composed of flood plain foresets regarded as the Lower Coal

measures were deposited. Subsequently, the overlying Ajali Formation termed the false bedded

sandstones was deposited Obi (2000). This was followed finally by the deposition of Fluvio-deltaic

sediments that formed the Nsukka Formation around Okigwe.

Geological map of the sampled area. Triangle around Ezinachi (Modified after Onyekuru et al., 2018)

Figure 1: Map of the studied area, triangle showing the location of Ezinachi (Modified after

Onyekuru et al., 2018).

MATERIALS AND METHODS

Thirteen outcrop samples were collected at 1m intervals from the shale exposures close to the Clay

products factory(GPS: N05° 44.761, E007° 21.755)(Fig. 1) in Ezinachi Imo State Nigeria during two field

trips in April and August, 2013, coordinates were taken with Garlux 70 GPS. The samples were placed in

sterile plastic bags, taken to the laboratory of the department of Biological Sciences, Redeemer’s

University where they were sorted and later prepared according to the method of Durugbo (2010). The

samples for palynofacies were not oxidized so as to retain the original colour of the palynomorphs and

phytoclasts (Oboh-Ikuenobe et al., 2005).The samples were analyzed using a Zeiss Axioskop 2

microscope with an attached Axiocam 1Cc 1 Camera. The data was later plotted with TILIA and the

sample- by- sample occurrences of the different palynomorphs were plotted (Fig. 2). The camera was

used to take photomicrographs of some of the common palynomorphs at the palynology laboratory of the

Evolutionary Studies Institute of the University of Witwatersrand, Johannesburg, South Africa (Fig. 3).

All the palynomorphs present were counted and recorded in analysis sheets to enhance the dating and




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paleoenvironmental reconstruction. The unprocessed samples, residues, CD copies and duplicate prints

are housed in the palynological collections of the department of Biological Sciences, Redeemer’s

University, Ede, Osun State, Nigeria.

RESULTS

Pollen and spores

The productive samples yielded moderate records of palynomorphs totaling 673. The microflora is

composed of twenty four pollen species with a total count of seventy seven (79)(Table 1) made up of

sparse records of Ephedripites multicostatus, Proteacidites dehaani, Longapertites marginatus, L.

vanendeenburgi, Proxapertites operculatus, P. sulcatus, Psilamonocolpites medius, Retidiporites

magdalenensis, Echitriporites trianguliformis; Nine spores with a total count of 123, mostly contributed

by Laevigatosporites sp., and Deltoidospora adriennis together with Cyathidites minor, Verrucatosporites

sp., Cicatricosisporites sp., Polypodiaceoisporites sp., Selaginella myosorus with relicts of

Distaverrusporites simplex and Lycopodiumsporites sp.

Table 1: Total and percentage of recovered palynomorph groups

Palynomorph Group Total %

Total Pollen 79 11.74

Total Spores 123 18.28

Total dinoflagellate cysts 35 5.2

Acritarch 3 0.44

Microforaminiferal wall lining 3 0.44

Tasmanites 2 0.30

Algae 2 0.30

Total diatom frustules 35 5.2

Total fungal elements 391 58.1

Grand Total 673 100




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Figure 2: Ezinachi Clay Palynomorph distribution chart (TILIA Plot)




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Marine elements

Sparse records of dinoflagellates characterized the analyzed Ezinachi Clay samples. Altogether fourteen

dinocyst species with a total count of thirty-five were recovered. These, particularly, comprise sparse

records of Cordosphaeridium spp. (C. exilimurum, C. fibrospinosum, and C. inodes), Homotryblium

tenuispinosum, H. abbreviatum, Operculodinium centrocarpum, Spiniferites ramosus, S. pseudofurcatus,

Achomosphaera sp., Cleistosphaeridium sp., Thalassiphora sp., Hystrichokopolpoma cf. poculum, in

association with one acritarch (Leiosphaeridia sp.) with a count of 3, two microforaminiferal wall linings

and two tasmanites. The dinocysts were mostly at 7m, 9m and 10m. Microforaminiferal wall linings

occurred only at 3m and 12m.

Algae and Miscellaneous palynomorphs

Freshwater algae Botryococcus braunii occurred sparsely, together with common diatom frustules.

However, abundant fungal elements (total count of 391) especially species of Glomus, Dictyosporites,

Dicellaesporites, and Multicellaesporites characterized the studied samples.

Palynological zonation

Based on occurrence of palynomorphs, three palynological Assemblage zones (PAZI-III) were erected for

the studied section of the Ezinachi Clay.

PAZ I (13-11m)

This is the basal zone, the base of this informal zone was marked at 130m, the last sample analyzed in the

Ezinachi clay samples. The microfossil assemblage is characterized by spot occurrences of Proxapertites

operculatus, Cyathidites minor, Deltoidospora adriennis, Lycopodiumsorites sp., Laevigatosporites spp.,

Verrucatosporites sp., Sealginella myosorus, Retimonocolpites sp, Retitricolporites sp., and the

dinoflagellate cyst Spiniferites ramosus. These occurred in association with diatom frustules and

moderate fungal elements dominated by Glomus and hyphae. This assemblage suggests sediment

deposition in a shallow marine environment.

PAZ II (11-4m)

This is the richest interval in the studied section of the Ezinachi clay. Common records of Ephedripites

multicostatus, Longapertites marginatus, Retidiporites magdalenensis, Retimonocolpites medius,

Lycopodiumsporites sp., Proteacidites dehaani, L. vanendeenburgi, Proxapertites operculatus, P.

sulcatus, Echitriporites trianguliformis, Cyathidites minor, Deltoidospora adriennis, Lycopodiumsorites

sp., Laevigatosporites spp., Cicatricosisporites sp., Polypodiaceoisporites sp., Triporoletes sp., and

common records of the dinoflagellate cysts Cordosphaeridium inodes, C. fibrospinosum, C. exilimurum,

C. minimum, Homotryblium tenuispinosum, H. abbreviatum, Spiniferites ramosus, Operculodinium

centrocarpum, Polysphaeridium subtile, Lejeunecysta sp., Hystrichokolpoma sp., Achomosphaera sp.,

Cleistosphaeridium sp., the acritarch Leiosphaeridia spp., Microforaminiferal wall linings, co-occurring

with common fungal elements, diatom frustules and rare freshwater algae. This assemblage suggests

sediment deposition in a shallow to marginal marine environment with irregular incursion of freshwater.

PAZ III (4-1m)

The palynological assemblage within this uppermost section of the Ezinachi clay is characterized by

Echitriporites trianguliformis, Longapertites marginatus, Proxapertites operculatus, L. vanendeenburgi,

Proteacidites dehaani, Retimonocolpites medius, Spinizonocolpies echinatus, Monocolpopollenites sp.,

Monoporites annulatus, with spot occurrences of the dinoflagellate cysts Lejeunecysta sp.,

Palynofacies

The phytoclasts are dominated by unstructured phytoclasts, and structureless/degraded pytoclasts to

varying degree. Amorphous organic matter of both terrestrial and marine origin were encountered with

the marine being more common in samples 6, 7, and 8 which also yielded appreciable numbers of




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Fig. 3 (A-Y): Explanation to Figure 3: Photomicrographs of some of the palynomorphs recovered

from the Ezinachi Clay samples. A, Longapertites marginatus Van Hoeken-Klinkerberg, 1964,

5m(L45/3). B. Proxapertites operculatus Germeraad, Hopping and Muller, 1968, 10m (D48/2). C.

Laevigatosporites haardtii, 3m (V42/3). D. Fungal spore Dicellaesporites sp., 8m (V45/2). E.

Leoitriletes adriennis Potonié Gelletich Krutzch 1959, 9m (Y38/2). F. Verrucatosporites sp. 11m

(M42/3) G. Longapertites marginatus Van Hoeken-Klinkerberg, 1964, 7m (G36/1). H. Leiosphaeridia sp.

8m (P45/0). I. Proxapertites sulcatus Jaramillo 2007, 10m (P28/3). J. Diatom frustules, 2m (N52/3). K.

Spiniferites pseudofurcatus (Klumpp, 1953) Eisenack, 1963 Sample 8 (U56/2). L. Cordosphaeridium

fibrospinosum Davey and Williams 1966 Sample 7 (N39/4). M. Cordosphaeridium inodes (Klumpp,

1953) Eisenack, 1963 Sample 10 (F34/2). N. Diatom frustule , 11m (P35/0). O. Laevigatosporites sp.

11m (Q30/3). P. Cordosphaeridium inodes (Klumpp) Sarjeant, 1970, 9m (P48/4).Q. Cicatricosisporites

sp. 3m (R45/4). R. Cordosphaeridium exilimurum Davey and Williams 1966 Sample 8 (S38/3). S. Fungal

spore Glomus sp. 2m (S54/3). T. Homotryblium tenuispinosum Davey and Williams 1966b, 9m (M36/2).

U. Echitriporites trianguliformis P. M. van Hoeken-Klinkenberg. 1964 5m (G46/2). V.

Monocolpopollenites sp., 11m (G29/4). W. Homotryblium plectilum Drugg and Loeblich Jr. 1967 Sample

9 (L45/2). X. Retitricolporites sp., 5m (D28/3). Y. Fungal spore Dicellaesporites sp. Sample 8 (V45/2).




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dinoflagellate cysts and microforaminiferal test linings likely suggesting more defined periods of marine

transgression.

Micropaleontology

An attempt was made to study the foraminiferal contents of the samples to support the inferred age.

Unfortunately all the samples were barren. This could have arisen from the fact that outcrops were used.

DISCUSSION

Among the few recovered pollen were relicts of typical Nigerian Paleocene-Eocene pollen species and

spores especially Longapertites vanendeenburgi, L. marginatus, Proxapertites operculatus, Proteacidites

dehaani, Retidiporites magdalenensis, Distaverrusporites simplex, Echitriporites trianguliformis,

Retistephanocolpites williamsi, Arecipites microreticulatus, Ericipites pachyexinus, Bacutriporites

orluensis, E.trianguliformis, Retistephanocolpites williamsi, and Cicatricosisporites sp.

(Salami,1983,1990; Durugbo, 2013). Salami (1983) in studying the Upper Senonian (Maastrichtian) and

Lower Tertiary (Paleocene-Eocene) pollen grains from southern Nigeria had recorded Longapertites

vanendeenburgi, L. marginatus, Retidiporites magdalenensis, Retistephanocolpites williamsi, Arecipites

microreticulatus, Ericipites pachyexinus, Bacutriporites orluensis, E. trianguliformis among the younger

palynomorphs which co-occurred with Proteacidites dehaani, Constructipollenites ineffectus, Nigeripollis

gemmatus, Auriculiidites reticulatus and Mauriitides crassibaculatus some of which were among the few

recovered palynomorphs from the Ezinachi Clay samples. Likewise, in 1990, he further recovered most of

these from the “Lower Coal Measures” of the Anambra Trough, southwestern Nigeria. Durugbo(2013)

had also reported the presence of most of the afore mentioned palynomorphs together with dinoflagellate

cysts especially Palaeoperidinium pyrophorum which he used to confirm the presence of Late Paleocene

sediments in the Nsukka formation exposure at the Enugu-Port Harcourt express junction at Okigwe,

South Eastern Nigeria. Eisawi and Shrank (2008) had also associated L. marginatus, Foveomonocolpites

bauchiensis, Racemonocolpites facilis, Monocolpites marginatus, Syncolporites marginatus with the

Paleocene and Proxapertites operculatus, Cicatricosisporites dorogensis, Spinizonocolpites echinatus,

Mauritiidites crassiexinus, Echitriporites trianguliformis, Retistephanocolpites williamsi, and

Bacutriporites orluensis with the Eocene of the Melut Basin in Sudan.

Jan du Chene and Adeniran (1985) had recovered Cordosphaeridium exilimurum, C. multispinosum,

Ifeycta pachyderma, Fibrocysta lappacea, Phelodinium magnificum, Apectodinium homomorphum, A.

paniculatum, A. hyperacanthum, A. quinquelatum, A. summissum, Lentinia orei, (Lejeunecysta spp.),

Adnatosphaeridium membraniphorum, A. multispinosum, Achomosphaera alcicornu, Eocladopyxis

paniculata, Diphyes spinulum, Kallosphaeridium orchiesense, K. yorubaensis, Muratodinium fimbriatum,

Hystrichokolpoma rigaudiae, H. granulatum, H. fenestratum, Homotryblium abbreviatum,

Heteraulacysta granulata., H. pustulata, Spiniferites spp., Polysphaeridium zoharyi, Wetzeliellia

africaensis, Wilsodinium nigerians, Paleocystodinium golzowense, Deflandrea wardenensis and

Tithyrodinium evittii, from Late Paleocene – Early Eocene outcrops of the Imo shale along the Benin-Ore

Highway. However, only few of these were recovered from the Ezinachi Clay not with standing, Salard-

Cheboldaeff (1990) ranges for these pollen and spore species concurs with the Paleocene-Eocene age

reported by other workers mentioned earlier. Apart from the pollen and spores record, the dinoflagellate

cysts assemblage also support the proposed age. Wall et al., (1977) had associated the last down- hole

occurrence of H. tenuispinosum with the Middle Paleocene. Again, Durugbo (2013) had equally used the

presence of such dinoflagellate cyst as Palaeoperidinium pyrophorum to confirm the presence of Late

Paleocene sediments in the Nsukka formation exposure at the Enugu-Port Harcourt express junction at

Okigwe, South Eastern Nigeria. Unfortunately P. pyrophorum as well as other common Late Paleocene to

Eocene peridinoids such as Apectodinium homomorphum, A. quinquelatum, A. paniculatum which




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Bankole (2007) had associated with the Middle Paleocene- Eocene of the Oshosun Formation, Dahomey

Basin Nigeria were absent in the Ezinachi Clay samples. Generally, peridinoids were absent from the

studied samples indicating more marine environments since peridinoids are mostly associated with

shallow water inner neritic/ low salinity environments. A review of the ranges of the dinocyst recovered

from the Ezinachi Clay are highlighted below. Mehrota et al. (2012) had highlighted the ranges of

Cordosphaeridium gracile and C. fibrospinosum as Early Campanian-Late Oligocene and early

Maastrichtian-Rupelian (Early Oligocene) respectively. They further assigned a Valanginian-Basal

Lutenian (Middle Eocene) range for Oligosphaeridium complex. Kurita and McIntyre (1995) had also

recovered Cordosphaeridium fibrospinosum from Paleocene sediments from Manitoba in Canada.

Furthermore, from the Paleocene-Eocene Wilcox formation Louisiana Gregory and Hart (1995) had

reported the presence of Cordosphaeridium inodes, C. diversispinosum, and C. minimum. Bujak et al.,

(1980) had also recovered Cordosphaeridium exilimurum, C. diversispinosum, C. multispinosum, C.

cracenospinosum, C. divergens, and C. funiculatum together with various peridinoids from the Eocene of

Southern England.

Powell (1992) had given the ranges of Cordosphaeridium inodes, Cordosphaeridium fibrospinosum as

Danian to Priabonian (Early Paleocene – Late Eocene) and Ypresian to Lutetian (Early –mid Eocene)

respectively. Again, Stover et al, (1996) gave the range of Cordosphaeridium fibrospinosum from

England as Early Maastrichtian – mid Rupelian (Oligocene) while C. funiculatum ranged from Lutetian to

Late Rupelian (Eocene).

Edwards (1999) had recovered Cordosphaeridium gracile from Paleocene sediments in Pakistan. Again,

Oboh-Ikuenobe et al. (1998) had recovered Cordosphaeridium inodes, C. exilimurum, from the Late

Maastrichtian sections of the Cretaceous-Paleocene sediments from the Côte D’Ivoire- Ghana Transform

Margin West Africa. Again, Jaramillo and Oboh-Ikuenobe (1999) reported the presence of C. inodes from

the Upper Eocene-Lower Oligocene of Southern Mississippi and Alabama, U.S.A. Again, from the Late

Maastrichtian and Paleocene strata from Northern Mississippi embayment southern Missouri, Oboh-

Ikuenobe et al., (2012) had also recovered Cordosphaeridium exilimurum, C. fibrospinosum and C.

inodes. Furthermore, from the Eocene London Clay, Jolley and Spinner (1989) had also recovered

Cordosphaeridium spp., and Homotryblium spp.. Conclusively, Mbesse et al. (2012) had outlined the

ranges of about thirty stratigraphically significant dinoflagellate taxa from various wells recovered from

oil exploration activities in the Douala Basin Cameroon. They gave the ranges of Cordosphaeridium

inodes, C. minimum, C. multispinosum, and Homotryblium tenuispinosum in Nigeria as Late Cretaceous

to Paleocene, Late Cretaceous to Eocene, Paleocene –Early Eocene and Late Paleocene- Eocene

respectively.

Again, the absence of other common Middle Paleocene to Eocene dinoflagellate cyst such as

Apectodinium homomorphum, A. quinquelatum, A. paniculatum could have arisen from environmental

conditions especially salinity regimes. This scarcity of Apectodinium and other peridinoids coupled with

records of such gonyaulacoids as Cleistosphaeridium sp., and Spiniferites sp. supports an outer neritic

water depth (Gregory and Hart, 1995). Again, Cordosphaeridium spp., have been associated with open

sea conditions (Downie et al., 1971; Islam, 1984; Köthe, 1990), Edet and Nyong (1993) had also

associated the preponderance of peridinoids to shallow water environments. The preponderance of

dinoflagellate cyst which were mostly gonyaulacoids in few samples (7,8,9) could be attributed to brief

periods of marine transgressions which agrees with the reports of Umeji and Nwajide (2007) that there

were more marine conditions in the Southern part of the Nsukka Formation to which Okigwe and its

environs belong. Hence, the Ezinachi Clay could have been deposited during the terminal part of the

Middle Paleocene transgression in the Anambra Basin which was followed by the deposition of the Imo

Formation which is of Middle Paleocene to Eocene age (Durugbo, 2013).




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Environment of deposition

This assemblage suggests sediment deposition in a dominantly nearshore environment in which these

species thrived due to the abundant records of pteridophyte spores and fungal elements which grow well

in coastal environments. Furthermore, the preponderance of dinocysts of gonyaulaoid affinities in some

samples, together with fungal elements, diatom frustules and rare freshwater algae coupled with the

phytoclasts which were dominated by structureless organic matter with scanty structured and unstructured

phytoclasts supports a nearshore shallow marine condition. However, the common records of gonyaulaoid

dinoflagellate cysts and rare peridinoids indicates sediment deposition in a dominantly shallow marine

environment with brief period of deepening and more open marine conditions (Edet and Nyong, 1993).

Notwithstanding, Edwards (1998) had also inferred a nearshore marine environment of deposition for the

Paleocene Black Mingo Group in South Carolina from which she recovered Cordosphaeridium

fibrospinosum, along with numerous peridinoids such as Apectodinium homomorphum, Palaeoperidinium

pyrophorum, Spinidinium pulchrum, Achilleodinium biformoides, Isabelidinium viborgense, Lejeunecysta

sp., Phelodinium sp., etc

Conclusion

Based on the findings of this present study and coupled with the presence of Homotryblium

tenuispinosum, and numerous Cordosphaeridium species a late Paleocene to Eocene age is hereby

proposed for the Ezinachi Clay pending further investigations from other disciplines. The environment of

deposition was dominantly nearshore /shallow to marginal marine.

Acknowledgements

We are grateful to Emeka Durugbo, Solomon Ijeoma, Obiawuchi Okwum for assisting during the sample

collection. Our profound gratitude also goes to Prof. Marion Bamford of the Evolutionary Institute,

University of the Witwatersrand Johannesburg South Africa for the use of Tilia and lab space for analysis

and the use of photomicroscope.

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