Heavy Mineral Distribution in the Lokoja and Patti Formations, Southern Bida Basin, Nigeria: Implications for Provenance, Maturity and Transport History

S. I. Bankole 1 , A. Akinmosin 1 , T. Omeru 1 ,  and H. E. Ibrahim 1
  • 1 University of Lagos, Faculty of Science, Department of Geosciences, Akoka, Lagos, Nigeria
S. I. Bankole
  • Corresponding author
  • University of Lagos, Faculty of Science, Department of Geosciences, Akoka, Lagos, Nigeria
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, A. Akinmosin
  • University of Lagos, Faculty of Science, Department of Geosciences, Akoka, Lagos, Nigeria
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, T. Omeru
  • University of Lagos, Faculty of Science, Department of Geosciences, Akoka, Lagos, Nigeria
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and H. E. Ibrahim
  • University of Lagos, Faculty of Science, Department of Geosciences, Akoka, Lagos, Nigeria
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Abstract

Heavy mineral component of 13 samples from the Lokoja and Patti Formations, Bida Basin have been studied for their textural characteristics, compositional abundance, maturity and provenance determinations. The suite of heavy minerals encountered is classified as opaque and non-opaque constituents. The non-opaque components include zircon, tourmaline, rutile, garnet, staurolite, epidote, kyanite, titanite, lawsonite, cassiterite, sillimanite, hornblende, hypersthene and andalusite. The assemblage is generally dominated by zircon and tourmaline in the two formations. The constituent heavy minerals identified are dominated by ultra-stable and stable classes, whereas the ZTR indices indicate mineralogical immaturity coupled with textural immaturity of the constituent grains. This suggests the possible dominance of chemical weathering of the source rock. The suites of minerals recovered have been linked to both metamorphic and non-metamorphic crystalline rock origins.

Introduction

The Intracratonic Bida Basin (Nupe or Middle Niger Basin) is one of the inland sedimentary basins of Nigeria [1], located roughly at the mid-central Nigeria (Figure 1). It is a north-west-southeast trending basin contiguous with the Anambra Basin. It extends from Kontagora, Niger State to Dekina, Benue State with a length of about 400 km and a width approximating 160 km [2]. Sediment accumulation in the basin commenced from Campanian and continued through the Maastrichtian [3] with fills ranging between 3.5 and 4.5 km thickness [4, 5] at the central part of the basin. Several research papers have been published on the evolution and stratigraphy of the basin.

Figure 1
Figure 1

Geological map of Nigeria. Box indicates the study area.

Citation: Materials and Geoenvironment 66, 3; 10.2478/rmzmag-2019-0011

Rift origin in connection with the aulacogen Benue Trough of Nigeria consequence to the separation of the South American and African continents in the Late Jurassic has been suggested for the Bida Basin [6, 7, 8]. This rifting resulted in the generation of series of horst and graben structures that characterizes the floor of the Bida Basin.

On the basis of geographical and lateral facies variation, the basin has been divided into the northern and southern sub-basins (Figure 1). In the southern Bida sub-basin, the oldest sedimentary unit, lying non-conformably on the Precambrian to Lower Paleozoic crystalline basement complex is the fluviatile Lokoja Formation (Figure 2). Patti Formation conform-ably overlies the Lokoja Formation (Figure 3). Observations at the base of Agbaja Plateau and also at the Ahoko Village mine indicate mixed marine and continental deposition environments for the Patti Formation. Literature accounts revealed that the formation consists of sandstones, siltstones, mudstones and shale in intercalation with bioturbated ironstones [9, 10]. The marine series of the Patti Formation is exposed at an abandoned mine in Ahoko Village along Lokoja-Abuja Highway. This unit, which constitutes part of the shale member of the Patti Formation has been extensively reviewed, described and reported by several authors [8, 10, 11, 12, 13]. The Agbaja Ironstone Formation caps the sequence of sediments in the southern Bida Sub-basin. Agbaja Formation is an intercalation of claystones, sandstones and oolitic/massive ironstones. Ladipo et al. [14] interpreted the sequence of the formation as abandoned channel sands and overbank deposits with marine influence resulting in the formation of the massive concretionary and oolitic ironstones.

Figure 2
Figure 2

Section of the Lokoja Formation exposed at Okumi, along the Lokoja-Abuja Highway.

Citation: Materials and Geoenvironment 66, 3; 10.2478/rmzmag-2019-0011

Figure 3
Figure 3

Section of the Patti Formation exposed near the Agbaja Plateau along Lokoja – Agbaja road. The capping rock (uppermost section) in this outcrop is the lower unit of Agbaja Ironstone Formation.

Citation: Materials and Geoenvironment 66, 3; 10.2478/rmzmag-2019-0011

In the present study, we report on the distribution and concentration of heavy minerals in the Lokoja and Patti Formations. On the basis of these, attempt is made to infer the provenance, maturity and transport history of the sediments of the formations. Detrital sediments are products of pre-existing igneous, metamorphic and also sedimentary rocks. These rocks are composed of diverse detrital minerals with some being classified as placer minerals. The latter are generally highly mechanically resistant and survive the usual complex transportation processes from source areas to the depocenters. These characteristics have allowed the use of heavy minerals in the study of sediment provenance, maturity and transport history. This method has been widely applied in fluvial [15, 16], coastal-shallow marine [17, 18], deep marine [19] depositional environments.

Materials and Methods

Materials

In total, 13 sediment samples (six from Lokoja Formation and seven from Patti Formation) were subjected to heavy mineral analysis. The analysis was carried out at the Sedimentological Laboratory, Department of Geosciences, University of Lagos, Nigeria.

Methods

Heavy mineral analysis in this study followed the procedure of Suzuki [20] and Mange and Maurer [21] for heavy mineral separation. The heavy liquid, Bromoform (CHBr3) with a density of 2.9 g/cc and viscosity of 0.068 poises was used. The samples were air-dried for a week to dispel any moisture as they were collected during the rainy season. Thereafter, the sediments were gently disaggregated by squeezing between fingers and filter paper or mortar and pestle in the case of hard samples to liberate individual grains. Each sample of 70 g was weighed and sieved to obtain 62.5–500 microns size grains. The individual sample was then poured into the bromoform and stirred thoroughly to free the samples of air bubbles. The particles were allowed to settle for about 20 minutes, stirring periodically to prevent the particles from adhering to funnel wall. The heavy crop was repeatedly washed in excess acetone and distilled water and air-dried and labelled. In all, 13 permanent mounts were made on slides using coupled resin. Mineral identification on the basis of their optical properties as proposed by Mange and Maurer [21] and Lindholm [22] was conducted on the samples.

More than 100 grains were counted from each slide for statistical analysis. Rock fragments, unidentifiable grains as well as authigenic and opaque minerals were excluded from the total sum to obtain uniform, comparable data on transparent assemblages for the characterization of mineralogical provinces. The sum of transparent minerals was recalculated to a value of 100% and the abundance of each heavy mineral species was scaled accordingly. The “ZTR” index which is the combined percentage of zircon, tourmaline and rutile among the non-opaque heavy minerals, omitting micas and authigenic species was calculated using [23] formula below:

ZRTindex=Zircon+Tourmaline+RutileNonopaque×100

ZTR index was calculated for the samples to ascertain their mineralogical maturity. According to Hubert [23], ZTR index <75% implies immature to sub-mature sediments and ZTR >75% indicates mineralogically matured sediments.

Results and Discussions

Results

Heavy mineral concentration in the Lokoja and Patti Formations is classified into opaque and non-opaque constituents. The opaque components generally referred to as iron stained heavy minerals require further chemical analysis to allow investigation under petrographic microscope. This chemical analysis, however, is beyond the scope of the present investigation and no further serious attention apart from statistical consideration is accorded to this class of heavy minerals herein. The recovered non-opaque components common to the two formations include the following: zircon, tourmaline, rutile, garnet, staurolite, epidote, kyanite, titanite, lawsonite, cassiterite, sillimanite, hornblende, hypersthene and andalusite (Plates 1–14). Kyanite, cassiterite, hypersthene, staurolite, hornblende and lawsonite show rare occurrences in the Lokoja Formation, except in a sample (Lok2 S6) that has significant amount of hornblende. Also, Kyanite, titanite, hornblende and garnet show rare occurrences in the Patti Formation, kyanite occurs only in PAT S7 sample. The proportion of heavy mineral recovered to the volume of sediment analysed is generally low and may not support any significant economic prospect. Information on the proportion of the heavy minerals recovered from the two formations is provided in Tables 1 and 2. Also, Tables 3 and 4 show the calculated ZRT% index results.

Table 1

Proportion (number of grains) of heavy minerals concentration in the sediments of Lokoja Formation.

Sample

Name
S/NZrnTurRtGrtStEpSilTtAndKyMCstHblHypLwsOpq
LOK1

S1
14314-4-4--4----22
LOK1

S2B
251311-8112739---3236
LOK1

S4B
35434122-5-4----142
LOK2

S2
41193815331-6-11-253
LOK2

S6
56342-3--3--471-245
LOK2

S8
669512102108-3-2---31560
TOTAL1003724294322491932548262458

Note: Zrn = Zircon; Tur = Tourmaline; Grt = Garnet; St = Staurolite; Ep = Epidote; Sil = Sillimanite; Tt = Titanite; And = Andalusite; Ky = Kyanite; Opq = Opaque, Hbl = Hornblende; Hyp = Hypersthene; Cst= Cassiterite; Lst = Lawsonite; M= Mica. S/N: Serial Number.

Table 2

Proportion (number of grains) of heavy minerals concentrations in the sediment samples from Patti Formation.

CODES/NZrnTurRtGrtStEpSilTtAndKyMHblOpq
PAT S1B127101-42113--1303
PAT S2B213112--4-3--8354
PAT S5B344216-2-3-4-201
PAT S741092413108482-41352
PAT S135-------------
PAT S166-------------
PAT S17B73481--2-4---2420
TOTAL573815623161381821284330
Table 3

ZTR maturity index and individual percentage mineral of the sediment samples of Lokoja Formation.

CODEZrnTurRtGrtStEpSilTtAndKyMCstHblHypLstTOTAL NON-OPAQUEZ+T+RZTR% INDEX
LOK1

S1
4314-4-4--4----24833.3
LOK1

S2B
51311-8112739---3631930.2
LOK1

S4B
5434122-5-4----301240.0
LOK2

S2
1193815331-6-11-522344.2
LOK2

S6
6342-3--3--471-331339.4
LOK2

S8
69512102108-3-2---31248669.4
TOTAL10037242943224919325482632616149.4
%30.711.37.48.91.29.87.42.85.80.97.71.22.50.61.8Individual abundance mineral%

Average ZTR% Index = 42.8%

Total Opaque = 2458

Total Non-opaque = 326

Total Non-opaque excluding micas = 301

Table 4

ZTR maturity index and individual percentage mineral of the sediment samples of Patti Formation.

CODEZrnTurRtGrtStEpSilTtAndKyMCstHblHypLstTOTAL NON-OPAQUEZ+T+RZTR% INDEX
PAT

S1B
27101-42113---1--503876.0
PAT

S2B
13112--4-3--8-3--442659.1
PAT

S5B
44216-2-3-4----261038.5
PAT

S7
1092413108482--4--742128.4
PAT

S17B
3481--2-4------221568.2
TOTAL5738156231613818212-8--21611050.9
%26.417.66.92.810.67.46.03.78.30.95.6-3.7--Individual abundance mineral%

Average ZTR% Index = 54.0%

Total Opaque = 4330

Total Non-opaque = 216

Total Non-opaque excluding micas = 204

The summary of the identification/classification criteria and the significant characteristics of each of the recovered heavy mineral are as follow:

Zircon: Zircon grains (Plates 2, 3 and 6) are prismatic, rounded to sub-rounded and sometimes contains fluid and mineral inclusions. Prismatic grains frequently showed zonation identified by fine bands parallel to the crystal boundary (Plate 2). The colourless varieties are more in abundance than the coloured varieties. The grains are easily identifiable owing to their very high relief and they are surrounded by black halo (Plates 2, 3 and 6). They show weak pleochroism and strong birefringence.

Tourmaline: Tourmaline grains (Plates 1, 2, 4 and 5) are prismatic, elongated, oval-shaped, spherical, euhedral, sub-hedral to irregular in shapes, with terminations at one or both ends of prismatic variety. Moderate relief, mineral inclusions (Plate 9) and overgrowths were frequently observed (Plate 1). Colours vary from pale to pink, dark green (Plate 4), pale yellowish, dark brown (Plate 4), very dark (almost opaque, may be iron bearing; Plates 1 and 5) and sometimes colourless. Colour zoning is frequent, pleochroism sharp and distinctive. Varicoloured varieties were also present (one portion of the grain displays striking different shades to the other).

Rutile: Rutiles (Plate 7) appeared as small and sub-rounded slender prisms with well-developed terminations or breakage patterns. A thick halo surrounds the grains because of their extremely high refractive indices. Grains are mostly brownish red to brownish black in colours and show distinct pleochroism (Plate 7).

Kyanite: Kyanite grains (Plates 8 and 12) are angular, or prismatic, dominantly colourless, weakly pleochroic (uneven coloured pleochroism) and exhibit characteristic cross-fractures and step-like features (Plates 8 and 12). The step-like uneven thickness resulted in a spectacular arrangement of the interference colours appearing in blue and grey on thicker and thinner parts, respectively.

Sillimanites: Sillimanites (Plates 9, 11 and 13) are long, slender, prismatic or irregular in shapes. Sillimanites show distinct cleavage, pleochroic (pale brown to pale yellow), parallel extinction, shows brilliant second- and third-order interference colours with yellow, green and pink as a dominant shades; slight twinkling is noticeable on rotation.

Andalusite: Andalusite (Plates 2–4, 6 and 7), mostly colourless and frequently enclose carbonaceous impurities. The rare manganoan variety, viridine which is green in colour was observed (Plate 4). They occur as prismatic, sub-rounded to angular or of irregular morphology; cleavage traces are poorly displayed. Some grains are non-pleochroic, whereas others display inhomogeneous pattern of pleochroism. Due to their irregular shape and uneven thickness, they display disorderly patterned interference colours. Weak interference colours are second-order orange and greenish blue (Plates 2–4, 6, and 7).

Garnet: Garnets (Plates 1, 3–6), easily identifiable because of their high relief and isotropic nature are euhedral, rounded, sub-rounded or irregular grains with uneven or conchoidal fractures. Colours vary from pinkish brown, pale red, pale pink to colourless.

Titanite: Titanite (Plate 12) grain has a high resinous lustre. Relief shows a slight twinkling on rotation of the stage. The grain has a weak pleochroism and good cleavage. High-order interference colours in golden yellow and yellowish white.

Staurolite: Staurolite (Plates 4, 11 and 14) occurs as irregular or angular grains. Colour ranges from pale yellow, golden yellow to dark yellowish brown. They exhibit distinct pleochroism (colourless to different shades of yellow).

Epidote: Epidote (Plates 2, 6 and 8) occurs as irregularly shaped grains, yellowish green to green coloured with fairly high relief. They exhibit distinct pleochroism (colourless, pale yellow, yellowish green).

Discussion

The percentage proportions of the non-opaque heavy mineral constituents (Figures 4 and 5) in Lokoja and Patti Formations show the dominance of zircon. Tourmaline is the second most abundant of the recovered minerals. Epidote comes next in the Lokoja Formation with staurolite in the Patti Formation. Epidote is present in all the samples of the Lokoja Formation but only in three (3) samples of the Patti Formation. Staurolite was recovered in three (3) samples each of the Lokoja and Patti Formations. The minerals with the lowest percentage proportion are cassiterite, staurolite, kyanite and hypersthene in the Lokoja Formation, whereas the lowest in the Patti Formation is kyanite. Cassiterite, lawsonite and hypersthene are totally absent in the Patti Formation. In the heavy mineral stability index of [24,25], hornblende, hypersthene and andalusite are classified as unstable, epidote, kyanite, garnet, sillimanite, titanite, lawsonite, cassiterite as moderately stable, garnet, staurolite as stable and zircon, tourmaline, rutile as ultra-stable minerals. Consequent to the proportion of the constituent heavy mineral in the studied sections, the sediments of the Lokoja and Patti Formations are considered generally stable as they are dominated by ultra-stable and stable minerals.

Figure 4
Figure 4

Overall percentage proportion of each non-opaque heavy mineral in the Lokoja Formation.

Citation: Materials and Geoenvironment 66, 3; 10.2478/rmzmag-2019-0011

Figure 5
Figure 5

Overall percentage proportion of each non-opaque heavy mineral in the Patti Formation.

Citation: Materials and Geoenvironment 66, 3; 10.2478/rmzmag-2019-0011

The calculated ZTR% index for the two formations ranges from 30.2% to 69.4% in the Lokoja Formation (Figure 6), whereas in the Patti Formation, it ranges from 28.4% to 76.0% (Figure 7). All, except one sample from the Lokoja Formation, have ZTR% index of <50%. This low ZTR index indicates that the samples of the Lokoja Formation are mineralogically immature. The ZTR index of the Patti Formation shows only slight improvement with two samples having ZTR >50% and three having ZTR% index of <50%. The mean percentage of ZTR index for Lokoja Formation is 42.8%, whereas that of Patti Formation is 54.0%. These show the comparative mineralogical maturity advantage of the sediments of the Patti Formation over their Lokoja counterparts.

Figure 6
Figure 6

Bar chart of ZTR index of each selected samples of Lokoja Formation.

Citation: Materials and Geoenvironment 66, 3; 10.2478/rmzmag-2019-0011

Figure 7
Figure 7

Bar chart of ZTR index of each selected samples of Patti Formation.

Citation: Materials and Geoenvironment 66, 3; 10.2478/rmzmag-2019-0011

Generally, very few rounded grains were encountered in all the samples studied (Plates 1–14). Most of the grains are either angular or sub-angular, suggesting that the sediments are from nearby sources and may not have been transported far away from weathering location. Hence, indicating textural immaturity of the sediments of both formations.

The abundance of ultra-stable and stable heavy minerals in an assemblage of texturally immature sediments grains (angular to sub-angular) is suggestive of the prevalence of chemical weathering of the source rocks contributing the heavy minerals to the studied formations.

Based on the constituent minerals in the studied sediments, mixed source ranging from high-to low-grade metamorphic and non-metamorphic sources is suggested. The possibility of contribution from low-grade metamorphic and non-metamorphic sources is indicated with dominance of zircon and tourmaline [26] in the two formations. Mange and Maurer [21] have linked the presence of lawsonite, hypersthene, hornblende, cassiterite, kyanite, andalusite, sillimanite, titanite, epidote, staurolite, garnet to high-grade metamorphic terrain. Also, Diekmann and Kuhn [27] attributed the dominance of low maturity heavy mineral such as green hornblende and garnet to high-grade metamorphic source. Rutile is generally linked to high-grade metamorphic source.

Conclusion

Heavy mineral analysis of both Lokoja and Patti Formations shows the predominance of non-rounded heavy minerals suites indicating short transport history from the sediment source, probably the southwest and north central Basement Complex terrains. The ZTR indices gave a general evidence of immature sediment suites for the Lokoja and Patti Formations with the latter being more matured than the former. Furthermore, the sediments of both formations are stable as they are dominated by ultra-stable and stable minerals. An assemblage of stable heavy minerals in a suite of texturally immature sediments validates the prevalence of chemical weathering of the source rocks which contributed to Lokoja and Patti Formations. The source of the sediments from both formations is interpreted to be of igneous and metamorphic terrain as indicated by the dominance of zircon, tourmaline, rutile, mica and opaque components.

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  • [1]

    Obaje, N.G., Moumouni, A., Goki, N.G., Chaanda, M.S. (2011): Stratigraphy, Paleogeography and hydrocarbon resource potentials of the Bida Basin in north-central Nigeria. Journal of Mining and Geology, 47(2), pp. 97–114.

  • [2]

    Nwajide, C.S. (2013): Geology of Nigerian Sedimentary Basins. Awka: CSS Bookshop, pp. 227–340.

  • [3]

    Wright, J.B., Hastings, D., Jones, W.B., Williams H.R. (1985): Geology and Mineral Resources of West Africa. London: George Allen and Urwin, pp. 90–120.

  • [4]

    Udensi, E.E., Osasuwa, I.B. (2004): Spectra determination of depths to magnetic rocks under the Nupe Basin, Nigeria. Nigeria Association of Petroleum Explorationists Bulletin, 17, pp. 22–37.

  • [5]

    Ojo, S.B. (1984): Middle Niger Basin revisited: magnetic constraints on gravity interpretations. In: 20th Conference of the Nigeria Mining and Geosciences Society, Nsukka, pp. 52–53.

  • [6]

    King, L.C. (1950): Outline and distribution of Gondwanaland. Geological Magazine, 87, pp. 353–359.

  • [7]

    Kogbe, C.A. (1981): Geological interpretation of land-sat imagery of part of central Nigeria. Journal of Mining and Geology, 28, pp. 66–69.

  • [8]

    Braide, S.K. (1992): Syntectonic fluvial sedimentation in the Central Bida Basin. Journal Mining Geology, 28, pp. 55–64.

  • [9]

    Olugbemiro, R.O., Nwajide, C.S. (1997): Grain size distribution and particle morphogenesis as signatures of depositional environments of Cretaceous (non-ferruginous) Facies in the Bida Basin, Nigeria. Journal of Mining and Geology, 33, pp. 89–101.

  • [10]

    Akande, S.O., Ojo O.J., Erdtmann B.D., Hetenyi, M. (2005): Paleoenvironments, organic petrology and rock-eval studies on source rock facies of the Lower Maastrichtian Patti Formation, Southern Bida Basin, Nigeria. Journal of African Earth Sciences, 41, pp. 394–406.

    • Crossref
    • Export Citation
  • [11]

    Idowu, J.O., Enu, E.I. (1992): Petroleum geochemistry of some late Cretaceous shales from the Lokoja Sandstone of Middle Niger Basin, Nigeria. Journal of African Earth Sciences, 14, pp. 443–455.

    • Crossref
    • Export Citation
  • [12]

    Ojo, O.J., Akande, S.O. (2006): Sedimentological palynological studies of the Patti Formation, southeastern Bida Basin, Nigeria: Implications for palaeoenvironment and palaeogeography. Nigerian Association of Petroleum Explorationists Bulletin, 19(1), pp. 61–77.

  • [13]

    Ojo, O.J., Akande, S.O. (2009): Sedimentology and depositional environments of the Maastrichtian Patti Formation, southeastern Bida Basin, Nigeria. Cretaceous Research, 30, pp. 1415–1425.

    • Crossref
    • Export Citation
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    Geological map of Nigeria. Box indicates the study area.

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    Section of the Lokoja Formation exposed at Okumi, along the Lokoja-Abuja Highway.

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    Section of the Patti Formation exposed near the Agbaja Plateau along Lokoja – Agbaja road. The capping rock (uppermost section) in this outcrop is the lower unit of Agbaja Ironstone Formation.

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    Overall percentage proportion of each non-opaque heavy mineral in the Lokoja Formation.

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    Overall percentage proportion of each non-opaque heavy mineral in the Patti Formation.

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    Bar chart of ZTR index of each selected samples of Lokoja Formation.

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    Bar chart of ZTR index of each selected samples of Patti Formation.