ARID ZONE JOURNAL OF ENGINEERING, TECHNOLOGY &
ENVIRONMENT

AZOJETE June 2020. Vol. 16(2):351-362
Published by the Faculty of Engineering, University of Maiduguri, Maiduguri, Nigeria.

Print ISSN: 1596-2490, Electronic ISSN: 2545-5818
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ORIGINAL RESEARCH ARTICLE
GEOLOGICAL SETTING AND SOLID MINERAL POTENTIALS OF SOUTHERN

BORNO, NORTHEASTERN NIGERIA

S. Baba, B. Shettima and H.I. Kamale*
(Department of Geology, Faculty of Science, University of Maiduguri, P.M.B 1069 Borno State Nigeria)

*Corresponding author’s email address: ishakukamale@gmail.com; hikamale@unimaid.edu.ng

1.0 Introduction
The southern part of Borno state is located within longitudes 11º 40' 00"E and 14º 20' 00"E and
latitudes 10º 15' 00"N and 10º20' 05"N in northeastern Nigeria. It politically comprises of 8
Local Governments Areas of Askira-Uba, Biu, Chibok, Damboa, Gwoza, Hawul, Kwaya-Kusar
and Shani (Figure 1). Geographically, the area falls within the sudan savannah characterized by
short shrubs and few scattered trees, with short wet-season (June-September) and long dry
season (October-May). Topographically it is characterized by rugged terrain provided by the
Mandara (Pulka-Gwoza-Chibok) mountains and the Biu plateau (Figure 2). The geology of
southern Borno is typified by vast occurrence of Precambrian Basement Complex rocks in its
eastern region, whereas the western flank of the area is underlain by the Tertiary-Quaternary
basaltic rock of the Biu Plateau. Sedimentary rock of Albian-Tertiary age underlies the extreme
western region and locally associated with volcanic intrusions.

A number of solid mineral resources, particularly industrial/non-metallic types (examples are
feldspars, quartz, clays, dimension stones) and gem quality stones have been identified in the
area. Good quality feldspar with high triclinicity (Δ) value (Baba et al., 1991) has been mined
from Liga pegmatites in Gwoza area since 1985 for ceramic production while gem-quality
stones, including tourmaline, garnet and topaz have also been identified and mined from Gunda
area of Biu plateau in the 1990s (Baba, 2005).

This work intends to re-evaluate the geological setting of the area with the aim of further
differentiating the rock types in more detail as well and their structural framework and their
implications in possible mineralization processes. It also intends to re-examine the solid mineral
resources potentials of the different rock types in the area with the aim of harnessing the
exploration targets for possible exploitation.

ARTICLE
INFORMATION

ABSTRACT
This research work has principally succeeded in updating the geological map of
Southern Borno and brought out zeolite as one of the prominent solid minerals
to work on. The field mapping of the area constituting of Askira Uba, Bayo, Biu,
Chibok, Damboa, Gwoza, Hawul, Kwaya Kusar, and Shani Local Government
Areas indicate the occurrence of basement and sedimentary rocks. The
crystalline rocks comprises of migmatites, gneisses, granites and basaltic rocks,
dominantly occurring in Gwoza, Askira Uba, Chibok, Biu and Hawul, whereas the
sedimentary formations cover Kwaya Kusar, Shani, Bayo and Damboa with
outcrops of Cretaceous-Quaternary sediments comprising Bima Formation,
Gongila Formation, Fika Shales, Gombe Sandstone, Kerri Kerri Formation and
Chad Formation. Mineralogical evaluation of the Basement Complex rocks
indicate the occurrences of feldspars, quartz, micas and ornamental stones, with
the basalts chiefly hosting zeolite and quality gemstones (aquamarine,
corundum, amethyst, tourmaline and topaz). The zeolites are typical of
chabazite variety mostly developing from feldspathoid associated with mafic
igneous/basic volcanic rocks. The Cretaceous-Quaternary sediments present
quality clays, kaolinite, diatomite, trona and bentonite industrial minerals.

© 2020 Faculty of Engineering, University of Maiduguri, Nigeria. All rights reserved.

Submitted 14Oct., 2019
Revised 07March, 2020
Accepted 10March, 2020

Keywords:
Zeolite
Gemstones
Solid minerals
Southern Borno
Nigeria

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Arid Zone Journal of Engineering, Technology and Environment, June, 2020; Vol. 16(2) 351-362. ISSN 1596-2490;
e-ISSN 2545-5818; www.azojete.com.ng

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Figure 1: Political Map of Southern Borno

Figure 2: Topographic Map of Southern Borno

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Ankidawa et al: Hydrogeological and Engineering Investigations of Gully Sites in Zing and Environs, Northeastern Nigeria.
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Corresponding author’s e-mail address: ishakukamale@gmail.com; hikamale@unimaid.edu.ng 354

2. Materials and Methods
2.1 Geological Mapping
The southern part of Borno was mapped on a scale of 1:50,000 using topographic map as base
map. A total area of about 24,150 km2 was covered using traverse compass mapping technique.
Representative rock samples were chipped, described on the spot as hand specimen. Samples
were then labelled, the locations noted and plotted on the base map with the aid of the GPS
which gives exact coordinates of sample points in terms of latitudes and longitudes. The
megascopic features and characteristic field relationships of the formations, structural elements
as well as possible mode of occurrence of the various rocks and formations in the areas were
measured, described and recorded.

2.2 Thin section preparation
Rock and mineral samples collected from the field were taken to petrology and mineralogy
laboratory of Geology Department, University of Maiduguri and were thin sectioned following
the procedure outline by Kerr (1977) which involves cutting a thin slice from the rock samples
using cutting machines. The slices were polished with abrasive powder until a required
thickness of 0.03mm was attained. The polished surfaces of the slices were then mounted on
the glass slides using araldite. The glass slides with the mounts were placed on the hot plate and
heated for 10 minutes. The samples were removed from the hot plate and allowed to cool. The
slides were once more polished to standard thickness of 0.03mm using abrasive powder of
various grades on glass laps. Canada balsam drops were smeared on the glass slides while on
the hot plate and very thin glass covers were placed on the finished polished surfaces in which
gentle pressure were applied to remove trapped air bubbles as well as excess Canada balsam.
The slides were allowed to cool, hardened while the overflow of the balsam was washed off
using organic solvent. The slides were then properly labelled and subjected to petrographic
studies using petrological polarizing microscope.

3. Results and Discussion
3.1 Geological Setting
Field mapping reveals that southern Borno is underlain by Basement Complex rocks,
Cretaceous sediments and Tertiary-Quaternary volcanics (Figure 3).

Figure 3: Geological map of Southern Borno (Inset-map of Nigeria showing the location map)

3.1.1 The Basement Complex rocks:
The Basement Complex rocks constitute about 60% and outcrop dominantly in the eastern
part of the study area particularly in Pulka, Gwoza, Hambagda, Limankara and Chibok areas.
The Basement Complex rocks are Precambrian in age the evolution of which has been
attributed to four major orogenic episodes in Nigeria (Baba, 2005); the Liberian (2800±200 Ma),
the Eburnean (2000±200 Ma), the Kibaran (1100±200 Ma) and the Pan-African (600±150 Ma).
The whole of Africa was affected by the Liberian and Eburnean episodes but the Kibaran and

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Pan-African are not pronounced in some areas on the continent. In Nigeria, the Kibaran activity,
which was largely sedimentation and volcanism with subsequent metamorphism producing low-
grade, N-S trending, gold bearing metasedimentary schist belts, was restricted to the western
half of the country west of longitude 8o E (Baba, 2005). The Pan-African orogeny engulfed the
whole of Nigeria making it fall fully within the Pan-African mobile belt.

Rocks resulting from the Liberian and Eburnean episodes are represented by migmatite-gneiss
complex (MGC). These rocks are generally low-lying, highly deformed, petrologically confusing
and structurally gost-looking units. In southern Borno the MGC outcrops at the margins of the
prominent Mandara mountains in Pulka-Gwoza areas as well as Hambagda apparently
enveloping the mountain range. The Pan-African orogeny on the other hand is the most
extensive and widespread episode in Africa which has largely obliterated the footprints of the
older episodes. It resulted in the emplacement of large volume of granitic plutons which are
now generally referred to as “Older Granites” to distinguish it from the high-level Jurassic
granites of central Nigeria which is called “Younger Granites” (Falconer, 1911). Recently
however, the term “Pan-African Granitoids” is preferred by modern Nigerian geologists.

The Pan-African Granitoids in southern Borno vary in texture but are mineralogically similar
except a few subordinate basic variants. The dominant variants include coarse porphyritic
biotite granites (pink-feldspar and white-feldspar sub-variants), coarse grained granite, medium
grained granites and fine grained granites with subordinate but genetically important pegmatites,
aplites and dolerites. Fracturing and felsic veins (including the aplite) chacterize the closure of
the Pan-African activity in Nigeria (Islam et al.,1989).

The Cretaceous sediments
The sediments in southern Borno are part of the Cretaceous-Recent sediments in the Nigerian
sector of the Chad Basin. General sequence of the sediments include; Bima Formation, Gongila
Formation, Fika shales, Gombe sandstones, Kerri-Kerri Formation and Chad Formation (Fig. 3).
The Aptian-Albian Bima sandstone, encompasses the northern, western and extreme south
western parts of the area, a continental formation represents the oldest sedimentary
succession in the entire Northeast, which rests directly and unconformably on the Precambrian
crystalline Basement Rocks and consists of three siliclastic members: the lower Bima (B1),
middle Bima (B2), and upper Bima (B3) (Carter et al., 1963; Guiraud, 1990, 1991)). The
formation generally consists of massively bedded, sparsely fossiliferous, poorly sorted, medium-
coarse grained arenaceous feldspathic sandstone. It is mainly composed of sandstones, although
the occurrence of shale intercalations has been reported (Carter et al., 1963, Avbovbo et al.,
1986). The lithology is diverse, indicating accumulation under widely varying conditions,
including fluviatile, deltaic and lacustrine depositional environments (Carter et al., 1963; Allix,
1983; Guiraud, 1990).

The Lower Bima Sandstone is the oldest unit and was interpreted as a proto-rift and syn-rift
succession (Guiraud, 1990), which is a thick continental deposits being the infillings of semi-
isolated grabens, with a variable thickness ranging from 0 to greater than 1500m. The
sediments consist of poorly sorted, angular arkoses, granulestones, pebbles and boulder
conglomerates. Fresh fragments of acidic rocks are common. Red to mottled colours are
characteristic suggesting pedo-genetic features, and intercalations of volcanic rocks indicate
contemporaneous volcanic activity (Popoff, 1988).

The thickness of the Middle Bima Sandstone ranges from 100-150m, consisting of gravelly to
coarse-grained feldspathic sandstone dominated by large-scale trough and tabular cross bedding
and clays. Palaeosols may occur at the top of this unit. Guiraud (1990, 1991.) reported fossil
wood to which late Albian age was assigned.

The Upper Bima sandstone is fairly homogeneous and relatively mature fine to coarse-grained
sandstone with pebbly beds and rare bands of calcareous sandstones characterized by tabular
cross-bedding. Convulate bedding and overturned cross-bedding are common. Its thickness
ranges from 500-1500m.

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Ankidawa et al: Hydrogeological and Engineering Investigations of Gully Sites in Zing and Environs, Northeastern Nigeria.
AZOJETE,16(2):351-362. ISSN 1596-2490; e-ISSN 2545-5818, www.azojete.com.ng

Corresponding author’s e-mail address: ishakukamale@gmail.com; hikamale@unimaid.edu.ng 356

The Gongila Formation with outcrops restricted to the western half of the study area, overlies
the Bima Sandstone which was deposited in shallow paralic environment hence regarded as
transitional between the underlying continental Bima and full marine Fika Shale above. It
consists of basal limestone and interbeds of shale and sandstone giving a thickness of 1500m
(Hamza et al., 2002). The limestone is rich in ammonites and mollusc, these assemblages
indicates early Turonian age (Carter et al., 1963).

The Fika Shale with occurrences in western part of the study area around Balbaya (Fig. 3)
conformably overlies the Gongila Formation and it consists of a sequence of blue-black,
gypsiferous and ammonite-rich shales with occasional thin limestone beds. It has a thickness of
1190m (Hamza et al., 2002). Fish, ostracod and reptile remains have been reported which
supports Turonian-Santonian age (Carter et al., 1963; Kachroo et al., 2000).

The Gombe sandstone comformably overlies the Fika Shale with occurrences in the northern
portion of the study area notably around Damboa and Balagala areas. It consists of sandstones,
siltstones, mudstones and ironstones. It has amaximum thickness of 310m and it is of
Maastritchian age (Zaborski et al., 1997).

The Kerri-Kerri Formation was observed to occupy the northern part of the study area, a
purely continental deposit, comprises of grits and sandstones having well-developed cross-
bedding structures suggesting deltaic environment. It is distinctly characterized by reddish and
often capped by oolitic lateritic horizon. Based on field and palynological studies, a Paleocene
age was assigned to it with thickness of 320m (Dike, 1993).

The Chad Formation outcrops in the extreme northern part of the mapped area and is made
up of blue-grey, fine to coarse-grained sand, with intercalation of sandy clay, clay, grits, gravel
and diatomite. It is lacustrine and fluviatile in origin. Based on some vertebrates’ jaw bones and
diatoms the formation is Pliocene-Pleistocene in age (Barber and Jones, 1960).

3.1.3 The Volcanics
There are two areas of volcanic occurrence in southern Borno, the Biu plateau and the
Kirawaareas.Biu area was subjected to two volcanic eruptions, the Pliocene (5-3 Ma) and the
Quaternary (< 1.4 Ma) (Grant and Freeth, 1972). These eruptions are represented by two
compositionally similar but structurally different volcanic rocks, the “Biu type basalts and the
Miringa-type basalts” together forming the spectacular Biu-plateau. Biu plateau is the largest
area of volcanic rocks in Nigeria covering an area of about 500 Km2 (Carter et al., 1963) with
an average elevation of 700m.

The Biu basalts belong to the early eruption and from field evidence, it is believed to have
resulted from fissure (gentle) eruption now represented by extensive massive lava flows
covering the entire southern part of the plateau. The later eruption (Miringa-type) is associated
with violent eruption (vent-type) as evident by the occurrence of pyroclastic materials such as
volcanic bombs, pumice, welded tuff etc. around volcanic cones. The two ages of Pliocene and
Quaternary given by Grant and Freeth (1972) were further collaborated by the mineralogical
work of Islam (1986) where the olivine phenocrysts in the Biu-type basalts were found to be
usually altered, commonly to iddingsite, while those in the Miringa-types were relatively fresh.
The Biu-type basalts areessentially “alkali olivine basalts” while the Miringa-type are mainly
“basanites”.

Kirawa volcanics are also Tertiary in age and form part of the Cameroon-line in the
northeastern part of the study area. They are compositionally acidic as opposed to the basic
nature of the Biu-plateau volcanic. Okeke (1991) identified two variants of Kirawa volcanic as
“Commendites” and Pentellerites”.

The Pentellerites are homogenous rhyolitic lavas while the commendites are tufaceous. From
petrological point of view the commendites are younger as field evidence has shown them to
contain xenoliths of the pentellerites.

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3.2 Petrography
As stated above, southern Borno is underlain by Precambrian Basement Complex rocks,
Cretaceous sediments and Tertiary-Quaternary volcanics. Because of the preliminary nature of
this report, only the detail petrography of the basalts is presented.

Generally, the basalts consist of plagioclase feldspars, augite, olivines, nepheline, zeolite and
opaque minerals. The plagioclases occur both as phenocrysts and as groundmass. The
phenocrysts are colourless and subhedral in form with low relief and weak birefringence. They
shows white to gray interference colour of first order and exhibit a combined albite and
Carlsbad twinning (Figure 4) though some crystals show only albite twinning (Figure 5). The
crystals have perfect cleavage in two directions perpendicular to one another. Augite occurs as
pale green crystals having prismatic form of short dimensions. It has high relief and strong
birefringence with pale green to greenish interference colour of the second order. It shows
perfect cleavages in two directions normal to one another. Olivine occurs as large phenocrysts,
yellowish in colour and euhedral in form. Some crystals occur both as subhedral and anhedral
with high relief and strong birefringence. It shows pale blue to deep blue upper second order
interfence colours. It is characterized by numerous irregular but characteristic Y-shaped
fractures (Figure 6) and exhibits parallel extinction with evidence of alteration in most crystals.
The nepheline is turbid white coloured and short prismatic form. It has perfect cleavage in two
directions with low relief and weak birefringence which exhibits grey of first order interference
colour. It shows symmetrical extinction and occurs as small phenocrysts with rows of
inclusions in some crystals while some constitute the groundmass. Zeolite occurs as colourless
and tabular in form having imperfect cleavages in two directions. Relief is low and birefringence
is weak and shows gray to white first order interference colours (Figure 7). The mineral
appears to fill empty cavities in the rock indicating that it is secondary material and the variety
is recognized as chabazite variety. Pyroxenes occur dominantly in the groundmass where, at
places, they cluster together forming a unique concentration (Figure 8).

Figure 4: Photomicrograph of basalt showing phenocryst of plagioclase feldspar exhiting both
Carlsbad and albite twinning

Plg

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Ankidawa et al: Hydrogeological and Engineering Investigations of Gully Sites in Zing and Environs, Northeastern Nigeria.
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Figure 5: Photomicrograph of basalt showing plagioclase phenocryst in groundmass of olivine,
augite, plagioclase and nepheline

Figure 6: Photomicrograph of basalt showing phenocryst of olivine

Plg

Olv

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Figure 7: Photomicrograph of zeolite filling empty cavity of basalt

Figure 8: Photomicrograph of basalt showing pyroxene concentration (Prx conc.) in a
groundmass of olivine, augite and plagioclase

3.3 Mineralization
The various geological components of southern Borno are individually characterized by
different types of solid mineral potentials. The Basement Complex rocks are known to harbour
some industrial minerals such as feldspars, clays and ornamental stones among others. The

Zeo

Prx Conc.

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Ankidawa et al: Hydrogeological and Engineering Investigations of Gully Sites in Zing and Environs, Northeastern Nigeria.
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Corresponding author’s e-mail address: ishakukamale@gmail.com; hikamale@unimaid.edu.ng 360

Cretaceous sediments on the other hand also host good quality clays, kaolin, diatomite, trona
and bentonite. The Tertiary-Quaternary basalts host good quality gemstones and clays.
Because of the preliminary nature of this work only zeolite, occurring in the Biu-plateau basalts
has been treated petrographically.

3.3.1 Zeolite
Zeolite is a group of hydrated aluminosilicate minerals consisting of over forty (40) varieties. All
are of framework silicates (Figure 9a) containing open cavities capable of holding loosely
bonded large cations and water. They are complex tektosilicates containing 3D network of
SiO4and AlO4 tetrahedra linked to form channels, cages, rings or loops (Figure 9b). Because of
these channels and cages in their structures cations and water molecules pass in and out of
them without disruption.

A

B
Figure 9: Structures of zeolite, A: framework silicates and B: 3D network of SiO4and AlO4

tetrahedra linked to form channels

Each oxygen ion is shared by two Si4+. Some number of Si4+ may be replaced by Al3+ and the
charge deficiency is balanced by the introduction of N+, K+ or Ca2+. The open cavities are
responsible for the low density of zeolite. The general formula is:

(Na+, K+, 1/2Ca2+)xZ [(SiAlx)O2(x+y]z.nH2O (1)

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Occurrence of zeolites in southern Borno has been found to be within the basalts of the Biu
plateau. The zeolite occurs in two generations. The first generation appear as primary
constituent in the basalts and in some instances predate the late eruptions (Figure 10) where
the basalt is seen to cross-cut the zeolite. The second generation of the zeolite is secondary in
nature where it is seen to fill vesicles and cavities within the basalts (Figure 7), probably formed
by late hydrothermal processes.

Physical and petrographic analysis of the zeolite shows that the variety is whitish in hand
specimen with hardness of approximately 4 and specific gravity of about 2. In thin section the
variety is colourless in plane polarized light and rhombohedron in form. Birefringence is high
with grey to white interference colours and often zoned (Figure 7). These physical and optical
properties suggest that the zeolite in the Biu basalts is chabazite (CaAl2Si4O12.6H2O) variety
which is the most common and useful type. Other natural zeolite varieties include natrolite,
laumonite, stilbite and sodalite. The Biu zeolite variety (chabazite) is closely related to
feldspathoid associated with mafic igneous rocks/ basic volcanic rocks. Zeolites are industrial
minerals used as drying agents, catalysts and washing materials.

Figure 10: Photomicrograph of basalt showing zeolite being crosscut by groundmass of basalt

4.0 Conclusion
The landscape of the southern part of Borno State is characterized by Basement Complex
rocks and Sedimentary covers. The Crystalline Basement is prominent around Gwoza, Askira
Uba, Chibok and Biu which are differentiated into migmatites, gneisses, granites and basalt
rocks. The sedimentary units dominate Kwaya Kusar, Bayo, Shani and Damboa with
occurrences of Bima Formation, Gongila Formation, Fika Shales, Gombe Sandstone and Chad
Formation.

The Basement Complex rocks host feldspar, Quartz, Mica mineralization and ornamental
stones. The basaltic rocks are composed of zeolite mineralization and Gemstones comprising
of Aquamarine, Corundum, Amethysts, Tourmaline and Topaz. The Cretaceous-Quaternary
sedimentary rocks are rich in quality clays, kaolinite, diatomites, trona and bentonite industrial
minerals.

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AZOJETE,16(2):351-362. ISSN 1596-2490; e-ISSN 2545-5818, www.azojete.com.ng

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