Figure 2. Cretaceous-Tertiary transgressions (T1-T6) in the Iullemmeden basin, modified from Greigert (1966) and Alzouma (1994).
distinguished two marine transgressions of Late Cenomanian and Early Turonian, respectively, by the presence of Neolobites vibrayeanus and Nigericeras.
However, Meister et al. (1991, 1992) found these same two species in the Late Cenomanian in nearly the whole Iullemmeden Basin, and thus concluded that a single transgression occurred during the Late Cenomanian and Early Turonian. Hence, five marine transgressions are now considered for the Marine Series, which are detailed in the following sections.
2.1. Mont Iguella Formation, the White Limestone and the Overlying Unit
The Late Cenomanian-Early Turonian transgression of Meister et al. (1991, 1992) deposited the Mont Iguella Formation in the Iullemmeden basin. It is a calcareous and siliciclastic succession that consists of thinly bedded, gray to yellow, fine to medium, often carbonaceous sandstones, intercalated with gypsiferous gray shales and yellow marly limestones (Alzouma, 1994). Its base corresponds to the fluviatile sandstones of the Continental Intercalaire. The associated fossils include lamellibranches, gastropods, echinoids and ammonites. The second, Late Turonian-Coniacian transgression of Meister et al. (1991, 1992) is marked by Coilopoceras inflatum and shaly limestone that Greigert (1966) named as the White Limestone Formation. In the area west of Abalak, this is marked by a prominent topographic feature, where mottled purple-green siltstones are capped by a marly gray limestone, which in turn is overlain by a massive, chert veined, white, recrystallized limestone (Moody and Sutcliffe, 1991). Above the White Limestone is a marly limestone (Overlying Unit) that is relatively rich in fossils (dinosaur and crocodile bones, fish teeth, etc.).
2.2. Majia Group
The third and fourth marine transgressions occurred during the Campanian-Lower Maastrichtian and Upper Maastrichtian, respectively, and were marked by Libycoceras. The Maastrichtian period was marked by the deposition of the Majia Group in western Niger; its lateral equivalent in the Sokoto area of Nigeria is called the Rima Group. The Majia Group consists of the Alambanya, Farin Doutchi, and Inwagar formations. These are respectively named the Taloka, Dukamaje, and Wurno formations in the Sokoto sector. The Taloka is also called the Lower Sandstones and Mudstones, the Farin Doutchi is called the Mosasaurus Shale, and the Inwagar is called the Upper Sandstones and Mudstones. In the Dakoro area, the Marine Series is overlain by the Taloka Formation, which consists of white fine-grained friable sandstones and siltstones with thin intercalated mudstones and carbonaceous shales. Thick Quaternary aeolian sands overlie these units, making outcrops very scarce, and the subsurface geology is unveiled only by borehole data.
During Upper Paleocene, the fifth marine transgression deposited the Garadoua Formation, which is equivalent to the Sokoto Group in Nigeria. The members of the Garadoua Formation are the Kao, the Tamaské and the Barmou from base to top. These correspond to the Dange, Kambaina and Gamba units, respectively, in the Sokoto Group. The base of the Garadoua Formation is observed in Garadoua village (Figure 3) and is made of slightly indurated bluish-gray shale, interbedded with thin layers of yellowish-brown limestone as the Dange Unit. Greigert (1966) called the base and the top of the Garadoua Formation “Schiste papyracé” (papyraceous shale) because of the very fissile nature of the two horizons. This formation has been mined for cement both in Niger and Nigeria for decades for the quality of the limestone it contains and the clay and gypsum potential of the underlying Farin Doutchi or Dukanmaje Formation. The fauna are very diverse and include bivalves, echinoids (Linthia soudanensis), gastropods, nautilus and foraminifera (Ranikauthalia). The Marine Series is well exposed in the Tahoua area of Niger as seen below (Figure 3).
The general geological map of the Iullemmeden basin established by Greigert (1966) and modified by successive researchers is presented below (Figure 4).
3. Materials and Methods
A total of 32 ditch cutting samples of shale facies from boreholes were collected from three different localities namely Kaya, Dandadji and Tahoua. The area covered represents the central part of the depocenter of the Marine Series of the Iullemmeden basin in Niger. These include 13, 10 and 9 samples from Kaya, Dandadji and Tahoua boreholes respectively (Figure 4 and Figure 5).
Figure 3. Outcrops of the marine series in tahoua area of niger.
Figure 5. Litho-logs and sampling points.
All the analyses were carried out at the University of Kentucky, Kentucky State, USA. All the samples had been ground in an agate mortar and sieved to 0.125 mm size. Major and trace elements were analyzed using a Bruker Tracer IV energy-dispersive hand held x-ray fluorescence spectrometer at the Pioneer Laboratory of the Department of Earth and Environmental Sciences. The XRF gun is fitted with a 40 keV and 60 μA X-ray tube. Chemical data were collected over 90 seconds in order to maximize the signal-to-noise ratio. Marked sample points were analyzed twice, once each for major and trace element chemistry, respectively. Major elements with atomic number 11 - 26, were collected at 15 keV and 35 μA under vacuum conditions of 9 torr. Trace elements, with atomic number 20 - 51, were collected at 40 keV and 15 μA, without a vacuum. The rock chosen as a reference material was SARM-41, a shale standard from South Africa (Ring, 1993). SARM-41 was run at the beginning and end of each three foot core box, in order to determine stability and reproducibility of the ED-XRF. Raw counts collected by the gun were calibrated and converted to elemental weight percentages using Bruker proprietary software and the empirical calibrations of Rowe et al. (2012). The calibrations of Rowe et al. (2012 ) were determined by comparing results of various analytical measurements (e.g., ICP-MS and WD-XRF) to the compositions of a suite of 90 mudrocks. Accuracy of the measurements decreases for lighter elements, such as sodium and magnesium.
Samples were analyzed for total inorganic carbon using a CM5014 coulometer (UIC, Joliet, IL, USA) and for total carbon and sulfur using the LECO SC-144DR instrument at the Kentucky Geological Survey (KGS). Total organic carbon was calculated by subtraction of inorganic carbon from the total carbon. For the mineralogical analyses, 11 of the samples (4 from Kaya, 4 from Dandadji and 3 from Tahoua) were analyzed using a Bruker AXS D8 Discover at the KGS.
4. Results and Discussion
4.1. Composition, Maturity and Palaeoweathering of the Marine Series
Cox et al. (1995)and Moosavirad et al. (2011)stated that the major element composition of fine siliciclastic rocks is usually controlled by clay minerals and non-clay silicate phases. Table 1 displays the values of major oxides of the Marine Series (mostly the shaly horizons). Silica is the most abundant constituent in all the samples with values range between 19.1 and 44.58 wt %. The next oxide in abundance is alumina (Al2O3) ranging between 8.17 and 4.15 wt % followed by Fe2O3 (3.27 - 18.23 wt %), CaO (1.10 - 11.20 wt %), SO3 (0.68 - 4.37 wt %), Na2O (0.66 - 1.37 wt %), TiO2 (0.50 - 1.40 wt %), K2O (0.05 - 1.51 wt %), MgO (0.17 - 0.62 wt %), P2O5 (0.06 - 0.44 wt %), MnO (0.05 - 0.29 wt %) and Cr2O3 (0.00 - 0.01 wt %).
In order to assess the composition, maturity and weathering of the sediments, geochemical indices such as the CIA, PIA, ICV and CIW have been computed as described by Nesbitt & Young (1982), Roser & Korsch (1988), Cox et al. (1995), Cullers (2000), and Hofmann et al. (2001):
CIA = 100 × [Al2O3/(Al2O3 + CaO* + Na2O + K2O)]
PIA = 100 × [(Al2O3 – K2O)/(Al2O3 + CaO* + Na2O – K2O)]
ICV = (Fe2O3 + K2O + Na2O + CaO + MgO + MnO)/Al2O3
CIW = 100 × [Al2O3/(Al2O3 + CaO* + Na2O)]
The values of CIA, PIA and CIW range between 23.02 - 75.1; 23.02 - 75.43 and 25.43 - 76.57 respectively (Table 2). Nesbitt & Young (1982) stated that CIA values are 0 for diopside; 30 to 45 for fresh basalts; 45 to 55 for granites and granodiorites; 50 for unaltered albite, anorthite and potassic feldspars; 75 for
Table 1. Major oxides of the Marine Series.
muscovite; 75 to 85 for illite, montmorillonite and beidellite; and close to 100 for kaolinite and chlorite. The CIA values found in most of the samples are below 75, the value of montmorillonite, which was identified as the major clay mineral in mineralogical analyses (Table 3). These CIA values could be underestimated as XRF has a very hard time measuring elements of low energy electrons like Na. hence, the XRD results could be more reliable here.
Table 2. Calculated geochemical ratios and indices of the Marine Series.
However, Cox et al. (1995) stated that values of K2O/Al2O3 ratio of clays are less than 0.3 and those of feldspars range from 0.3 to 0.9. The values of K2O/Al2O3 ratio of the Marine Series vary from 0.01 to 0.23 (Table 2) that is less than 0.3. These values also indicate preponderance of clay minerals over K-bearing minerals such as K-feldspars and micas (Cox et al., 1995).
In terms of maturity, CIA values plotted against those of ICV show that most of the samples are immature and have been subjected to weak weathering (Figure 6).
Table 3. Mineralogical composition of some selected samples of the Marine Series.
Figure 6. Plot of CIA versus ICV.
This could be also applied to mudrocks as a measure of compositional maturity because minerals show a relationship between resistance to weathering and ICV. Compositionally immature mudrocks that contain a high proportion of non-clay silicate minerals or that are rich in clay minerals such as montmorillonite and sericite will have high values of this index (>1). On the other hand, compositionally mature mudrocks that are poor in nonclay silicates or dominated by minerals such as those of the kandite family (kaolinite, halloysite and dickite) will have low values. Table 2 indicates that the values of ICV of the Marine Series range between 1.13 and 4.2 (>>1), consistent with compositional immaturity.
4.2. Paleoenvironment and Tectonic Setting
A binary diagram of SiO2 versus (Al2O3 + K2O + Na2O) shows that the Marine Series was deposited under wet/humid conditions (Figure 7). This is consistent with the findings of Pascal et al. (1991) and agrees with the hypothesis of generally high rainfall during the Cenomanian-Turonian (Parrish & Curtis, 1982), in accord with proximity to the equator (Rat et al., 1991).
Trace element ratios have been used as indicators of paleo-redox conditions, including V/Ni by Breit & Wanty (1991), Wanty & Goldhaber (1992), Peters & Moldowan (1993), Galarraga et al. (2008) and Cu/Zn by Hallberg (1976).
Similarly, Zhou & Jiang (2009) and Pi et al. (2014) stated that V is more effectively fixed in sediments containing organic matter in anoxic environments compared to Ni and Cr. Therefore, variations in the V/(V + Ni) and V/(V + Cr) ratios can be used to indicate oxygenation of the depositional environment, and higher V/(V + Ni) and V/(V + Cr) ratios indicate more strongly reducing conditions. According to Galarraga et al. (2008), a V/Ni ratio higher than 3 indicates that the organic matter was deposited under reducing conditions, while V/Ni ratios ranging between 1.9 and 3 indicate deposition under dysoxic to oxic conditions (mixed terrigenous and marine organic matter) and a V/Ni ratio < 1.9 indicates predominantly terrigenous organic matter.
From the analytical results of the Marine Series (Table 4), all the V/Ni values are less than 1.9 except for samples K61 (V/Ni = 2.12) and DJ9 (V/Ni = 10.56). All the values of Cu/Zn have their ratio lower than 1.9. The ratios V/(V + Ni) and V/(V + Cr) are either negative or positively low. All the above indicates dysoxic-oxic depositional environment. Rather, all the values of TOC (Table 4) are less than 2% except in sample DJ234 with value of 2.34 w%. So this explains that the preservation of the organic matter is consistent with the chemistry of rock.
Table 4. Some trace elements of the marine series.
To determine the provenance of siliciclastic sediments, McLennan et al., (1980) proposed a Ni versus TiO2 discrimination diagram and Floyd et al. (1989) used Al2O3 versus TiO2 plots. Most of the samples of the Marine Series plot in the acidic field of the Ni versus TiO2 diagram (Figure 8) and in the alkali granite-granodiorite field of the Al2O3 versus TiO2 plot (Figure 9), which implies that the sediments originated from acidic igneous rocks. From He et al. (2010)
and Dai et al. (2015), Al2O3/TiO2 ratio and SiO2 contents vary in the igneous rocks as follows: a) Al2O3/TiO2 were 3 to 8 in mafic igneous rocks (SiO2 content from 45 to 52 wt. %), b) Al2O3/TiO2 ratios were 8 to 21 in intermediate igneous rocks (SiO2 content from 53 to 66 wt. %), and c) Al2O3/TiO2 ratios were 21 to 70 in felsic igneous rocks (SiO2 content from 66 to 76 wt. %). The Al2O3/TiO2 ratios of most the studied sediments range from 4 to 13 implying that the source rocks of these sediments are intermediate igneous rocks.
The source of the sediments can be traced from the contiguous Aïr crystalline basement rocks in the north and the Zinder-Nigeria cristalline basement rocks in the South. Indeed, three periods of volcanism had been identified in previous studies ( Yahaya, 1992;
The present work shows that the Marine Series are made predominantly of clay minerals of the smectite group (montmorillonite), quartz and other accessory minerals like rutile and calcite. The sediments are immature and were deposited under dysoxic-oxic conditions which may justify the poor preservation of organic matter in the environment. In terms of origin, the sediments were derived from intermediate to acidic igneous rocks found adjacent to the basin. The occurrence of montmorillonite in the sediments by previous works is also confirmed in this study and the origin may be linked to the volcanic ash that evolved from volcanic eruptions that occurred in late Paleozoic-Mesozoic period in the North and South crystalline basement surrounding the basin. The bentonite potential and its source may be considered as a perspective investigation in the basin with the recent oil discovery success in Niger.
The analytical work was carried out at the University of Kentucky, USA by the first author who beneficiated from the Fulbright Fellowship. The Fulbright Foundation, the Staff of the Earth and Environmental Sciences Department as well as that of the Kentucky Geological Survey are all acknowledged for their respective assistance.
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