SEDIMENTOLOGICAL AND GEOCHEMICAL CHARACTERIZATION OF DF-2 WELL, ONSHORE WESTERN NIGER DELTA: IMPLICATIONS FOR PROVENANCE, TECTONIC HISTORY AND PALEO DEPOSITIONAL CONDITIONS

The sedimentology and geochemistry of the major oxides and trace elements of DF-2 well, Onshore, Niger Delta, are presented in this study. The study is aimed at describing the sedimentological characteristics as well as using the major oxides and trace elements to investigate the provenance, tectonic history and palaeo-depositional conditions of the well. Selected samples were investigated with fused bead X-Ray Fluorescence (XRF) spectrometry to determine their major oxides and fused bead laser ablation inductively couple plasma mass spectroscopy (LA-ICP-MS) for their trace elements. Sedimentological analysis from the well shows that the lithology ranged from shaly sand, sandy shale, sandstone and shale. The results show the dominance of silicon oxide (SiO2) contents which ranges from 81.1 to 91.4 wt. % (average of 87.1 wt. %). The low average concentration of Cr<150 ppm and Ni <100 ppm, the ratios of Th/Sc, Th/Co, Th/Cr, Cr/Th, La/Sc, as well as the plots of Th/Co versus La/Sc and TiO2 versus Zr, all infer a felsic source rock. The discrimination plots of ratioK2O/Na2O against SiO2 and Log K2O/Na2O against Log SiO2/Al2O3indicated passive continental margin. Various chemical classifications of the sediments show that the sandstone facies plotted mainly in quartzarenite, sublitharenite and Fe-rich sand domains. The samples were deposited under oxic environment based on the average values of U/Th (0.26 ppm), Ni/Co (2.79 ppm) and Cu/Zn (1.81ppm) and bivariate plot of Ni/Co versus V/Cr. However, the bivariate plot of Ni/Co versus V/ (V+Ni) specifies oxic to anoxic conditions and V/Vi + Ni ratios indicate oxic, suboxic to euxinicpalaeode positional environments for the sediments. Geochemical characterization illustrates mixed marine and terrigenous source input, deposited mainly in semi humid/humid climate. The positive values attained from ratios of Al2O3/(CaO+MgO+Na2O+K2O) infers mineralogical maturity based on stable mobile oxides content in the studied samples.


INTRODUCTION
The Niger Delta is situated on the Gulf of Guinea on the west coast of central Africa and extends throughout the Niger Delta Province as defined by Klett et al., (1997). It is one of the world's largest, deltas, with the sub aerial portion covering about 75,000 km 2 and extending more than 300 km from apex to the mouth (Doust and Omatsola, 1990).From the Eocene to the present, the delta has prograded southwestward, forming depobelts that represent the most active portion of the delta at each stage of its development (Doust and Omatsola, 1990, Fig. 1b).
According to Kulke, (1995), these depobelts, form one of the largest regressive deltas in the world with an area of some 300,000 km 2 . Hospers, (1965) indicated a sediment volume of 500,000 km 3 , and a sediment thickness of over 10 km in the basin's depocenter (Kaplan et al., 1994). The composition of siliciclasticfacies depends on the principal chemical composition of the source rock area and the tectonic history of the depositional basins (Das and Haake, (2003); Jin et al., (2006). Previous researchers such as; Cullers (2000); Cingolani et al., (2003); Armstrong-Altrin et al., (2004); Akinyemi et al., (2013); Chen et al., (2016); Mitra et al., (2018); Amiewalan and Lucas, (2020) among others, had worked on the Niger Delta sediments and other Basins to interpret their provenance, tectonic history, paleodepositional conditions and classification of associated sandstone facies. This study intends to use the major and trace element geochemistry to define the provenance, tectonic history, paleo-depositional conditions of sediments in the DF-2 well, offshore western Niger Delta .This will further enhance the already existing information in this region and would be of immense value to researchers and explorationists.

LOCATION OF STUDY AREA AND GEOLOGY
DF-2 well is located in Greater Ughelli Depobelt of the Niger Delta with geographic coordinates of Longitude E5 0 33' 36''.86 and Latitude N6 0 18' 25''.43. Fig  1b.According to Doust and Omatsola, (1990), the Niger Delta basin probably commenced in Albian time, after the opening of the South Atlantic Ocean and the break off of African and South American plates. The disintegration of the Central Africa-South America part of Gondwana happened during the Mesozoic along successions of rift zones of diverse location that met in a triple junction in the present-day Gulf of Guinea occupied by the Niger Delta. The two arms that followed the southwestern and southeastern coasts of Nigeria and Cameroon, advanced into collapsed continental margins of the South Atlantic, while the third, (failed arm)established the Benue Trough. The trough represents a failed arm of a rift triple junction accompanied with the opening of the South Atlantic. Lehner and De Ruiter, (1977), posited that rifting began in this region in the Late Jurassic and continued into the Middle Cretaceous. However, rifting diminished completely in the Late Cretaceous in the Niger Delta region. True Delta expansion started in the Late Paleocene/Eocene, when sediments began to build out beyond the trough between basement horst blocks at the northern flanks of the present Delta area, (Doust and Omatsola, 1990). The stratigraphy of the Niger delta has been controlled by the interplay between rates of sediment supply and subsidence. Eustatic sea-level changes and climatic variations have been the control on the sedimentation rate while the subsidence have been controlled essentially by initial basement morphology and differential sediment stacking on unstable shale. In numerous deltaic areas, it is challenging to delineate an adequate stratigraphic nomenclature, (Doust and Omatsola, 1990). Smaller number of lithofacies in the Niger delta makes it difficult to outline appropriate units and boundaries in establishing distinct Formations. However, three Formation names are widely use conforming to the sections of the tripartite sequences, stretching in age from Eocene to Holocene (Short and Stauble, (1967) ;Avbovbo, (1978);(Fig. 2) The subsurface Niger Delta sedimentary basin is subdivided into three stratigraphic units from the oldest to youngest namely; Akata Formations, Agbada and Benin Formations (Short and Stauble, 1967). The Akata Formation with Imo shale as the lateral equivalent is the basal unit of the Niger Delta. It composed mainly of marine shale facies with sporadic lowstandturbidite sand and minor amounts of clay and silt. Thin Akata sands are possibly of turbiditic origin and were deposited in delta-front to deep marine environments (Esan, 2002). The Formation is believed to be the main source rock within the Niger Delta complex. (Ekweozor, and Okoye, 1980;Bustin, 1988). The thickness ranges from 2,000 ft.
-20,000 ft. (600 m to 6,000 m) (Jev et al., 1993). Doust and Omatsola, (1990), estimated the age of the Akata Formation to be from Eocene to Recent. The Agbada Formation which overlies the Akata Formation has the Ogwashi-Asaba and Ameki Formations as their lateral equivalent. The Formation represents the fore set of the Niger Delta and comprised delta front lithofacies, consisting mostly of shoreface and channel sand deposits with minor shale in the upper parts and an alternation of sand and shale of almost equal proportion in the lower part. The clastics accumulated in delta-front, delta-topset, and fluvio-deltaic environments. It is the major petroleum-bearing unit of the Niger Delta (Reijers, (1996), which began in the Eocene and continues into the Recent. The thickness ranges from 9,600 ft. ft. (3,000 m -4,200 m) (Avbovbo, 1978). The Benin Formation, which is the youngest stratigraphic unit in the Niger Delta, mainly comprised non-marine sands with  XRF and LA-ICPMS analyses: Each of the twelve representative samples was pulverized and sample was placed in oven at 1000 0 C for 1 hour to determine loss on ignition (LOI) using a robotic TGA SEDIMENTOLOGICAL AND GEOCHEMICAL CHARACTERIZATION OF DF deltaic environments. It is the bearing unit of the Niger Delta (Reijers, (1996), which began in the Eocene and continues into the Recent. The thickness ranges from 9,600 ft. -14,000 , 1978). The Benin Formation, which is the youngest stratigraphic unit in the marine sands with a few shalyintercalations (Esan, 2002). The shale content increases towards the basal part of the Formation. continental deposit from latest Eocene to Recent, deposited in alluvial or coastal plain environments following a southward shift of deltai (Esan, 2002). The Formation is (Avbovbo, eighty two (382) ditch cutting 9650 ft. from DF-2 well were provided by the Nigerian Petroleum Development Company (NPDC) for this study. Detailed edimentological descriptions were carried out based on n as well as reflected light binocular light microscope on the samples to investigate the lithology, texture, color, and environmental sensitive minerals and

MATERIALS AND METHODS
The samples were composited and twelve representatives (DF1, DF2, DF3, DF4, DF5, DF6, DF7, DF8, DF9, DF10, DF11 and DF12 respectively) were log was established from the sedimentological description as shown in Fig. 3. The and fused bead laser ablation troscopy (LA-ICPwas carried out Bureau Veritas Minerals laboratory, Vancouver, Each of the twelve was pulverized and 20g of each C for 1 hour to using a robotic TGA system. 12.22 fluxes with 4% Lithium nitrate were added to the sample to form glass bead. determined by X-Ray Fluorescence oven dry temperature of 105 0 C. Supplementary analysis was carried out on the same samples using instrument to determine the trace elements composition of the sample. The laser of the instrument was used to evaporate the surface of the fused sample, the vapor and particles generated were conveyed by the carrier gas flow to the plasma of the ICP passed through the quadruple were detected and the data were quality check.LA-ICPMS analytical process to a single, cost effective fusion. Detection limits are similar to industry leading mixed acid trace element ICP-MS packages. The results of the major oxides are described as oxides percent by weight and trace elements quantified in ppm as shown in Tables 1 and 2. Both the Fluorescence (XRF) spectrometry for majoroxides composition and fused bead laser ablation inductively couple plasma mass spectroscopy (LA trace elements composition were carried out Veritas Minerals laboratory, Vancouver, Canada SEDIMENTOLOGICAL AND GEOCHEMICAL CHARACTERIZATION OF DF-2 WELL, ONSHORE WESTERN NIGER DELTA: few shalyintercalations (Esan, 2002). The shale content increases towards the basal part of the Formation. It is a continental deposit from latest Eocene to Recent, deposited in alluvial or coastal plain environments following a southward shift of deltaic environments up to 2,000 m thick. 1978).
Regional stratigraphy of the Niger Delta showing different Formations (after Ozumba, 2013).
. 12.22 fluxes with 4% Lithium nitrate were added to the sample to form glass bead. Major oxides were Ray Fluorescence Spectrometry on Supplementary analysis was carried out on the same samples using LA-ICP-MS instrument to determine the trace elements composition The laser of the instrument was used to the fused sample, the vapor and particles generated were conveyed by the carrier ICP-MS unit. The rays passed through the quadruple were detected and the ICPMS streamlines the a single, cost effective fusion. Detection limits are similar to industry leading mixed MS packages. The results of the major oxides are described as oxides percent by weight and trace elements quantified in ppm as shown in and 2. Both the fused bead X-Ray Fluorescence (XRF) spectrometry for majoroxides composition and fused bead laser ablation inductively couple plasma mass spectroscopy (LA-ICP-MS) for their trace elements composition were carried out at Bureau erals laboratory, Vancouver, Canada. Fig. 3 Simplified composite litho-log of DF-2 well, Western Niger Delta.

Lithostratigraphy
The sedimentological analysis ofDF-2 well logrevealed that the lithology ranged from sandstone, shaly-sand, and sandy-shale to shale. The studied sections was divided into two broad lithofacies sequences interpreted as the continental sequence (

) (Subunits A -C)
This interval is essentially a heterogeneous sequence of alternating sand and shale components, with the basal sample points (8270 ft. and 9480 ft.) predominantly composed of shale. The shale is Light grey, fissile, moderately hard. The sandstones are dark grey, fine to medium grained, sub rounded to rounded, poorly to well sorted. From the gross lithologic and grain attributes, the subrounded to rounded and well sorted sandstone indicating sediment maturity due to weathering and abrasion of the grains during transport. Index minerals are dominated by mica flakes with rare occurrences of shell fragment and ferruginous material. Most of the samples within this sequence are non-calcareous. The Continental sequence (5485 ft. -7270 ft.) (Subunits D -G) This is composed of alternating sequence of sandstone, shaly sand and relatively thin shale. The sands are brown, light to dark grey, fine to medium grained sized, sub angular to sub rounded and generally poorly to well sorted. The shales are grey, dark grey, platy to blocky and hard to reasonably tough. Index minerals are dominated by mica flakes with considerably occurrence of ferruginized material. The samples within this sequence are non-calcareous.

TRACE ELEMENTSGEOCHEMISTRY
The results of trace elements variation for the study well is shown in Table 2 Table 2: Trace Elements Composition of DF-2 Well.
The comparative abundance of trace elements in sediment is measured by sedimentation rate, terrigenous influx, biogenic influx, hydrothermal input, diagenesis and eventually, weathering (Leventhal, 1998). Some of these elements are depleted while others are enriched in relation to UCC and PAAS respectively(  , 1987).
The ratios of some important major oxides and trace elements for this study have been presented in Table 3 for further deductions of sediment source, tectonic setting, sandstone classification, maturity, paleooxidation as well as paleo-climatic conditions.

Sandstone Petrology
Using Herron (1988) diagram as shown in Fig. 4, majority of the DF-2 samples (70%) plotted mainly in the Fe-sand zone, indicating that they are ferruginous. The rest of the samples (30%) are scattered within the quartz arenite, sublitharenite and litharenite zones. Arising from Pettijohn (1972) plot of log (SiO 2 /Al 2 O 3 ) vs. log (Na 2 O/K 2 O) (Fig. 5), the studied samples plotmainly in quartz arenite with a few in sublitharenite zones. This may perhaps be the consequent of recycling/prolonged abrasion as well sedimentary influx from more than one source.    (Table 3), which is <1.5 and therefore less than the value for quartz arenite as proposed by Lindsey (1999). The average value of log (K 2 O/Na 2 O) for the sediments is 0.67, which is not in the greywacke range of Lindsey (1999). The average values obtained for log (SiO 2 /Al 2 O 3 ) is 1.24 and log (K 2 O/Na 2 O) is 0.67 whereas the average value of log ((Fe 2 O 3 + MgO)/(K 2 O + Na 2 O)) is 3.43. By this interpretation, the sediments cannot be categorized as Arkosein the concept of Lindsey (1999) criteria number three. The average values attained in this study relate with log (SiO 2 /Al 2 O 3 ) < 1.5 and log ((Fe 2 O 3 +MgO)/(K 2 O+Na 2 O)) > 0 of the fourth category. Accordingly, the sandstones in DF-2 well arelithicarenites. Lithic arenites usually contain 30-80% quartz and 5-50% lithic fragments. The compositional maturity can vary broadly depending on the nature of the lithic fragments. According to Folk ( 1974), lithic arenites are immature sandstones occurring as a result of high rate of sedimentation from supra crustal source followed by short transportation and are characteristics of fluvial or deltaic settings.

TECTONIC HISTORY
Several authors such as Maynard et al., (1982) ;Bhatia, (1983); Bhatia and Crook, (1986); Roser and Korsch, (1986); Kroonenberg, (1994) have developed classification schemes used to discriminate amongst sediments deposited in different tectonic settings. The cross plot of K 2 O/Na 2 O ratio against SiO 2 (Roser and Korsch, 1986) for this sediments, revealed that they all plotted in the Passive Continental Margin (PM) tectonic settings (Fig. 6). The plot of Log (K 2 O/Na 2 O) against Log (SiO 2 /Al 2 O 3 ) tectonic discrimination diagram of Maynard et al., (1982; Fig. 7), also indicates that the studied samples were deposited in the Passive continental margin (PM) field. Passive continental margins are highly prolific in hydrocarbon as they are related with favorable conditions for accumulation and maturation of organic matter (Obasi et al., 2015). According to Roser and Korsch (1986), passive margin sediments are largely quartz-rich which are derivative from stable continental areas where there are no active tectonic activity.  Taylor and McLennan, (1985) and as shown in Table 4, it can be ratios such as; Th/Sc, Th/Co, Th/Cr, Cr/Th and La/Sc are significantly different in felsic and basic rocks, which probably permit controls on the typical provenance. These ratios are related with sediments derived from SEDIMENTOLOGICAL AND GEOCHEMICAL CHARACTERIZAT of Roser and Korsch, (1986). Using K 2 O/Na 2 O ratio against SiO sediments.  Taylor and McLennan, (1985) and as shown in Table 4, it can be seen that such as; Th/Sc, Th/Co, Th/Cr, Cr/Th and La/Sc are significantly different in felsic and basic rocks, which probably permit controls on the typical provenance. These ratios are related with sediments derived from felsic and basic rocks, upper continental and PAAS values. From Table 3, the values of the various ratios and their averages are; Th/Sc (1.01 -2.30, -1.36, av. 0.89), Th/Cr (0.05 -(5.36 -18.38, av. 9.10) and La/Sc (0.57 4.33). From the above, the ratios of Th/Sc, Th/Cr, Cr/Th and La/Sc fall within the range of felsic rock while only Th/Co fall within mafic rock.
had posited that sensitive diagenetical trace elements such as Zr, Hf, Nb, Y, Sc, V, Cr, Cu, Co, Ni and Zn can infer provenance and environment of deposition owing to their fairly low movement during weathering, transport, diagenesis, and (1996), recommended that when Cr >150 ppm and Ni >100 ppm in abundance, they are indications of mafic or ultramafic source respectively. In this study, the average concentrations of Cr (70.92) and Ni (24.42) are low, confirming felsic rock as the source areas. This is further supported by Fig. 8, which shows cross plot of La/Sc versus Th/Co (Cullers, 2002) and Fig. 9, which indicates the cross plot of Zr versus TiO 2. (Hayashi et al., 1997), all pointing to felsic source rocks for the sediments. Cross plots of Zr versus TiO 2, for studied samples (after Hayashi et al.,1997).  (Cullers 2000) and mafic rocks (Cullers, 2000), UCC (Taylor and McLennan, 1985) and PAAS (Taylor and McLennan 1985).

Ranges of values in DF-2 well
respectively. In this study, the average concentrations of are low, confirming felsic rock as the source areas. This is further supported by Fig. 8 (Suttner and Dutta, 1986) specifies oxic condition during deposition of DF Fig. 11: Bivariate plot of Ni/Co versus V/ (V+Ni) (Rimmer, 2004) shows oxic to euxinic conditions during deposition of  (Nagarajan et al., 2007).Accordingly, the average low U content (average 2.02 ppm) of the DF

Paleo Oxygen Condition
Bivariate plot of Ni/Co versus V/Cr (Suttner and Dutta, 1986) specifies oxic condition during deposition of DF well sediment.
sensitive trace element (TE) ratios are among the major widely used indicators of redox conditions in recent and ancient sedimentary deposits. Trace elements such as U, Th, Cu, Zn, Ni, Co, V and Cr, give a better knowledge on the paleo redox conditions of sediments. High U concentration revealed sediments ) whereas low U content infers sediment deposited in oxidizing 2007).Accordingly, the average low U content (average 2.02 ppm) of the DF-2 well sediments favours an oxic condition during sediment deposition. During weathering sedimentary recycling, Th and U behave in a different way owing to the fact that U is chemically mobile and this action indicates a decrease in the ratio of U/Th. According to Nath et al., (1997), U/Th<0.75, it portrays oxic conditions values from 0.75 -1.25 specifies signifies suboxic to anoxic conditions (Table 5). Relating these values to DF-2 sediments, the U/Th ratios SEDIMENTOLOGICAL AND GEOCHEMICAL CHARACTERIZATION OF DF-2 WELL, ONSHORE WESTERN NIGER DELTA: Bivariate plot of Ni/Co versus V/Cr (Suttner and Dutta, 1986) specifies oxic condition during deposition of DF-2 Bivariate plot of Ni/Co versus V/ (V+Ni) (Rimmer, 2004) shows oxic to euxinic conditions during deposition of to define the paleo oxygenation condition of ancient sediments after Jones and (2015a).
well sediments favours an oxic condition during During weathering and sedimentary recycling, Th and U behave in a different way owing to the fact that U is chemically mobile and this action indicates a decrease in the ratio of U/Th. (1997), if the ratio of U/Th<0.75, it portrays oxic conditions of deposition, 1.25 specifies dyoxic, values >1.25 suboxic to anoxic conditions (Table 5). Relating 2 sediments, the U/Th ratios indicates low values from 0.20 -0.49 (av. 0.26; Tables 3), which confirmed deposition in oxic environment. According to Jones and Manning, (1994). The ratio of Ni/Co in DF-2 well varies from 1.56-4.81 with an average value of 2.79, and implies oxic environments of deposition (Table 3). Moreover, the Cu/Zn ratios could also be used as a redox proxy; low ratios reveals oxic conditions while high ratios deduce reducing depositional conditions (Deng and Qian, 1993). In the studied sediments, the ratio of Cu/Zn varies from 0.14 to 14.10 with an average of 1.53, and inferring deposition under oxic environments (Table 3).The bivariate plot of Ni/Co versus V/Cr (Suttner and Dutta, 1986;Fig. 10) designates oxic condition during deposition of DF-2 well sediments. This is further supported by the plot of Ni/Co versus V/ (V+Ni) (Rimmer, 2004;Fig. 11), which strongly amplify oxic conditions of deposition for the sediments. Wang, (1996), posited that when V/V+ Ni ratio is >0.84, it submits euxinic conditions, from 0.54 -0.82 characterize sanoxic condition, 0.46 -0.60 implies dyoxic conditions and <0.46 infers oxic condition. The V/Vi + Ni ratios for the samples ranges from 0.42 to 0.91 (average = 0.82), (Table 3) which indicate anoxic environment of deposition. As a result, the above constraints submit that the depositional conditions for the studied samples were oxic to euxinic. The Cross plot of vanadium versus nickel after Kafousia, et al., (2010), illustrates that the sediments had mixed marine and terrigenous source input and were deposited under oxic to dyoxic condition. Fig.  12. Fig. 12: The Cross plot of vanadium versus nickel of DF-2 samples from studied area shows that the sediments had mixed marine and terrigenous source input and were deposited under oxic to dyoxic condition (Modified after Kafousia, et al., 2010). SEDIMENTATION Potter, (1978), proposed SiO 2 /Al 2 O 3 as index used to illustrate the degree of sandstones maturity in comparison to mineralogical maturity. Maturity is shown best in quartz, rock fragments, feldspars and grain size determine by the quartz contents in the sediments, because quartz survives contrarily to feldspars, mafic minerals and lithics (Roser et al., 1996). According to Roser et al., (1996), values of SiO 2 /Al 2 O 3 ratio greater than 5.0 in samples suggest progressive maturity. Potter, (1978), opined that high ratios define mineralogically mature (quartzose rounded) samples, while low ratios denote chemically immature samples. The SiO 2 /Al 2 O 3 ratio for the studied samples varies from 6.14 -41.32 (av. 17.25) which is greater than 5.0. This infers that the samples are mineralogically mature with low content of fines/mudstone.Na 2 O + K 2 O (alkali content) indicates the amount of the feldspar content and likewise applicable as a guide for chemical maturity. The alkali content have range of values between 0.77 -1.79(av.1.07) which shows the presence of feldspars and low chemical maturity. The Fe 2 O 3 /K 2 O ratio ranges from 0.92 to 4.94 having an average of 3.70. The higher SiO 2 /Al 2 O 3 ratio and low Fe 2 O 3 /K 2 O ratio imply that they are mineralogically more stable and less prone to reactivity during supercritical CO 2 exposure. Farquhar et al., (2014). The obtained ratios for the studied samples are consequently mineralogically mature. Gill and Yemane, (1996), suggested that the ratio of Al 2 O 3 / (CaO+MgO+Na 2 O+K 2 O) can be used in defining the stability of mobile oxides. The positive value attained varies from 0.14 -5.20, inferring that there are stable mobile oxides in the studied samples. The bivariate plot of SiO 2 (revealing quartz content) versus (Al 2 O 3 + Na 2 O + K 2 O) (revealing of feldspar content) (Galarraga, et al., 2008) can be utilized in discriminating the palaeoclimatic condition during deposition. In this study, the samples all plotted in the humid climatic zone, (Fig. 13). This humid condition accelerated weathering processes and enhanced chemical maturity. Fig. 13: Bivariate plot of SiO 2 versus (Al 2 O 3 + Na 2 O + K 2 O) to discriminate palaeo-climatic condition during the deposition of the studied samples (Modified after Galarraga, et al., 2008).

CONCLUSIONS
Sedimentological analysis revealed four main lithofacies comprising of sandstone, shaly sand, shale and sandy shale. Geochemical results show that the average value of silica is far higher than the average values of the rest oxides. Silica enrichment is a measure of sandstone maturity, and is a reflection of the duration and intensity of weathering and destruction of other minerals during transportation. Trace elemental ratios of U/Th, Ni/Co, Cu/Zn and binary plot of Ni/Co versus V/Crindicated an oxic environment of deposition. However, the binary plot of Ni/Co versus V/ (V+Ni) showed oxic to euxinic environments of deposition. Trace elemental and major oxides ratios reveals passive continental margin, quartz arenite, sublitharenite, litharenite and Fe-rich sandstone derive from pre-existing igneous rock and the sediments had mixed marine and terrigenous source input deposited mainly in humid climatic condition. It can be inferred that the studied successions of the well were not affected by major tectonic activity.