A total of Twenty-one coal and carbonaceous shale samples were collected from four boreholes in Mamu and Awgu Formations of Lower and Middle Benue Trough, Nigeria. The samples were subjected to Elemental analysis using Gas Chromatography and Gas Chromatography- Mass Spectrometry (GC-MS).The saturated fraction was subjected to urea adduction to separate isoprenoids from n-alkanes and subjected to gas chromatography-mass spectrometry (GC-MS) using a CE 5980 GC coupled to an HP Finnigan 8222 MS held at 80oC for three minutes and raised to 310oC at 3oC min-1 and held isothermally for 10 minutes in order to assess some molecular parameters used in source rock characterization. The short chain/long chain saturated fatty acid (ATRFA) ratios for the samples which ranges from 0.85-1.00 and the carbon preference index (CPIFA) of the long chain n-fatty acids (C24-C30) ranging between 1.27 and 3.29 indicates both terrestrial and marine organic matter derived materials. The distribution of straight chain n-alkan-2-ones ranges from nC14 to nC33, maximizing at nC17 is an indication of contribution from higher plants.

1. Distribution of Possible Fatty Acids and Alkanones in some Thermally Immature Nigerian Coals
Distribution of Possible Fatty Acids and Alkanones in
some Thermally Immature Nigerian Coals
*1Uzoegbu M.U., 2Oghonyon R., 3Ugwueze C.U
1,2,3Department of Geology, Faculty of Science, University of Port Harcourt, Port Harcourt, Nigeria.
A total of Twenty-one coal and carbonaceous shale samples were collected from four boreholes
in Mamu and Awgu Formations of Lower and Middle Benue Trough, Nigeria. The samples were
subjected to Elemental analysis using Gas Chromatography and Gas Chromatography- Mass
Spectrometry (GC-MS).The saturated fraction was subjected to urea adduction to separate
isoprenoids from n-alkanes and subjected to gas chromatography-mass spectrometry (GC-MS)
using a CE 5980 GC coupled to an HP Finnigan 8222 MS held at 80o
C for three minutes and raised
to 310o
C at 3o
C min-1
and held isothermally for 10 minutes in order to assess some molecular
parameters used in source rock characterization. The short chain/long chain saturated fatty acid
(ATRFA) ratios for the samples which ranges from 0.85-1.00 and the carbon preference index
(CPIFA) of the long chain n-fatty acids (C24-C30) ranging between 1.27 and 3.29 indicates both
terrestrial and marine organic matter derived materials. The distribution of straight chain n-alkan-
2-ones ranges from nC14 to nC33, maximizing at nC17 is an indication of contribution from higher
plants.
Keywords: Alkanones, Benue trough, coal, Fatty acids, environment of formation Organic matter.
INTRODUCTION
Aliphatic wax lipids in the range ofC22-C32 were identified
as the major extractable components of angiosperm
leaves, barks and roots (Huang et al., 1995; Lockheart et
al., 2000; Kogel-Knaber 2002; Yuang and Huang, 2003).
Similar distributions have been reported in sediments and
macrofossils (Logan and Eglinton, 1994; Huang et al.,
1995, 1996; Lockheart et al.,2000). The functionalized
lipids are partly degraded during diagenesis (Bechtel et
al.,2001). The wax esters, their hydrolysis products, and
the free alkanol and fatty acids are preferentially degraded
to aldehyde, ketones and alkanes by microorganisms
(Puttmann and Bracke, 1995). These degradation
pathways favor short chain (<C20)n-alkanes that are
predominantly found in algae and microorganisms
(Cranwell, 1984).
Abundance of short-chain n-alkanoic acids and iso-
alkanoic acids reflect microorganism input (Otto and
Simpson, 2006). Vascular plants contribute significantly
long-chain (C16-C32) alkanols and alkanoic acids
(Barthlott et al., 1998) from waxes, suberin and cutin (Otto
and Simpson, 2006). Plant wax esters (C34-C72)are
typically composed of C20-C32 n-alkanols and C12-C30
n-alkanoic acids (Otto and Simpson, 2006).Generally,
short chain n-fatty acids (<C20) are believed to originate
from algae and microorganisms, whereas long chain
homologues are thought to be derived from higher land
inputs (Brown et al., 1972; Cranwell, 1974; Duan et al.,
1998).
There has been considerable interest in a series of long
straight chain acyclic ketones and a C18-isoprenoid
ketone which occur widely in ancient rocks, oil shales,
peats, coals, young sediments and living organisms
(Cranwell, 1977; Volkman et al.,1980b; Cranwell et al.,
1987; Lehtonen and Ketola, 1990; Rontani et al., 1992,
Tuoand Li, 2005). Long chain acyclic ketones are detected
as homologues series and usually show similar distribution
*Corresponding Author: Uche Mmaduabuchi Uzoegbu,
Department of Geology, Faculty of Science, University of
Port Harcourt, Port Harcourt, Nigeria. Email:
uche.uzoegbu@uniport.edu.ng
Vol. 6(1), pp. 103-110, August, 2019. © www.premierpublishers.org. ISSN: 9661-0255
Research Article
International Research Journal of Chemistry and Chemical Sciences

2. Distribution of Possible Fatty Acids and Alkanones in some Thermally Immature Nigerian Coals
Uzoegbu et al. 104
to alkanes (Tuo and Li, 2005). The n-alkan-2-ones, n-
alkan-3-ones and n-alkan-4-ones have also been detected
in lipid fractions extracted from aerosol particulate matter
(Simoneit et al., 1988, 1991), hydrothermal petroleum and
sediment extracts from Guyama Basin (Leif and Simoneit,
1995). The higher alkenones (>C25) homologues with a
high odd carbon number predominance were interpreted
to originate from vegetation wax by oxidation while the
lower homologues (<C25) with no odd or even Carbon
number predominance were thought to originate from
anthropogenic sources by combustion or exposure to high
temperature (Leif and Simoneit, 1995). The C37 andC38
diunsaturated methyl and ethyl ketones are
biosynthesized by a limited number of haptophyte bacteria
like Prymnesiophyte algae (Volkman et al., 1980; 1995),
Emiliania huxleyi (Sonzogoni et al., 1997; Schouten et al.,
2000) and Gephyrocapsa oceanica (Schouten et al.,
2000). Their distributions are now widely used as specific
indicators of past sea surface temperature (SSTs) and the
unsaturation ratios can provide a reliable indicator of the
temperature at which they are biosynthesized (Brassel et
al., 1986; Phral and Wakeham, 1987).
The 6,10,14-Trimethylpentadecan-2-one is quite common
in nature, occurringwidely in sediments, water particulate
matter and recently in coals (Volkman et al.,1983, Rontani
et al., 1992, Tuo and Li, 2005).These isoprenoid ketones
could be produced from free phytol by bacteria
degradation and photosynthesized oxidation,
photosynthesized oxidation of some isoprenoids
hydrocarbons and during photo degradation of -
chlorophyll (Tuo and Li, 2005).
The homologous series of alkan-2-ones is generally found
with an odd carbon number predominance and its source
is likely microbial (Leif and Simoneit, 1995; Bai et al.,2006).
It has been proposed that n-alkan-2-ones are formed by
microbially mediated -oxidation of alkanes (Cranwell et
al., 1987; Rieley et al., 1991; Simoneit et al., 1998;) or from
-oxidation and decarboxylation of n-fatty acids (Volkman
et al., 1983). n-Alkan-2-ones maximizing at C25 or C27
have been reported in higher plants, microalgae and
phytoplankton (Gonzalez-Vila et al., 2003; Bai et al.,
2006). This research aims in determining the possible type
of lipid and alkanones in some thermally immature organic
matter and determining the environment of formation of the
organic matter of Nigerian coals.
STRATIGRAPHIC SETTING
The infilling of the Anambra and Afikpo started during the
Campanian to the Paleocene (Danian) under two major
eustatic cycles; the more pronounced Nkporo
transgression and the less active Nsukka transgression
with the Anambra basin showing the most complete
stratigraphic sections (Fig. 1). These cycles are also found
in the Afikpo syncline SE of the Abakaliki anticlinorium and
the Dahomey embayment, west of the Ilesha basement
spur, although both are incomplete (Murat, 1972).
The first cycle which took place during the Lower
Campanian to the Maastrichian started with the deposition
of the Nkporo whose lateral (age) equivalents are the
Enugu and Owelli (Fig. 2). This is the basal unit of the
Campano-Maastrichian transgression and comprises of
dark mudstone, gray, fissile friable shales with thin beds of
marl, sandy shale and limestone overlying an angular
unconformity (Reyment, 1965).
The regressive phase was marked with the development
of a large offlap complex, starting with the paralic
sequence of the Mamu (Lower coal measure) overlying the
Nkporo (Reyment, 1965). It is thought to be lower
Maastrichian in age with a basal part that contains thin
marine intercalations, while the coal bearing part consist of
fresh water and low salinity sandstones, shale, mudstone
and sandy shales with coal seams occurring at several
levels (Simpson, 1955).
The Mamu formation is overlain by the continental
sequence of the Ajali. This sandstone unit has received
several names such as false bedded sandstone (Tattam,
1944), basal sandstone (Simpson, 1955) etc. iIts present
name was given by Reyment (1965) after establishing its
type locality at the Ajali. Virtually all exposures of the
formation are characterized by a lateritic profile at the top.
It was deposited during the regressive phase of the
Campano-Maastrichian transgression and the age is
Maastricthian.
The Ajali sandstone is overlain conformably by the Nsukka
Formation (Upper coal measures), and it consists of
alternating succession of gray sandy shales, sandstones,
plant bearing beds and thin beds of coal (Reyment, 1965).
Thin bands of marine limestone heralded the return of
marine sedimentation at the top of the formation. These
dark shales and the intensely bioturbated sandstones are
well exposed at Ihube, along the Enugu – Port Harcourt
expressway. The age range of the formation is late
Maastrichian to Danian based on the fossil record. This
formation bears the K/T boundary which is described by
Reyment (1965) as a period of transition in Nigeria. Mbuk
et al. (1985) identified this boundary in the Nsukka
Formation in Ozu Abam area of Abia State.

3. Distribution of Possible Fatty Acids and Alkanones in some Thermally Immature Nigerian Coals
Int. Res. J. Chem. Chem. Sci. 105
Fig. 1: Generalized geological map of Nigeria (boxed areas of inset) showing the geological map of the Anambra Basin.
Numbers indicate Cretaceous and Tertiary formations shown as follows: 1. Asu River Group; 2. Odikpani Formation; 3.
Eze-Aku Shale; 4. Awgu Shale; 5. Enugu/Nkporo Shale; 6. Mamu Formation; 7. Ajali Sandstone; 8. Nsukka Formation; 9.
Imo Shale; 10. Ameki Formation and 11. Ogwashi-Asaba Formation (after Akande et al., 2007).
Fig. 2: The Stratigraphy of the Anambra Basin Southeastern Nigeria (After, Ladipo, 1988 and Akande et al., 1992; Modified
in Uzoegbu et al., 2013b).
AGE
SEDIMENTARY
SEQUENCE
LITHOLOGY DESCRIPTION DEPOSITIONAL
ENVIRONMENT
REMARKS
ANKPA
SUB-
BASIN
ONITSHA
SUB-
BASIN
MIOCENE
OLIGOCENE
OGWASHI-
ASABA FM.
Lignites, peats,
Intercalations of
Sandstones &
shales
Estuarine
(off shore bars;
Intertidal flats)
Liginites
EOCENE AMEKE NANKA
FM. SAND
Clays,shales,
Sandstones
& beds of grits
Unconformity
Subtidal, intertidal
flats, shallow marine
PALEOCENE
IMO SHALE Clays, shales
& siltstones
Marine
MAASTRICHTIAN
Clays, shales, thin
sandstones & coal
seams
Coarse sandstones,
Lenticular shales,
beds of grits &
Pebbls.
Clays, shales,
carbonaceous
shale, sandy shale
& coal seams
NSUKKA FM.
AJALI SST.
MAMU FM.
? Estuarine
Subtidal, shallow
marine
Estuarine/ off-shore
bars/ tidal flats/
chernier ridges
CAMPANIAN
ENUGU/
NKPORO SHALE Clays & shales Marine
CONIACIAN-
SANTONIAN
AWGU SHALE
TURONIAN EZEAKU SHALE
Clays &
shales Marine
ODUKPANI FM.
CENOMANIAN
ALBIAN
L. PALEOZOIC
ASU RIVER GP.
B A S E M E N T C O M P L E X
Sub-
bituminous
Sub-
bituminous
3rd Marine
cycle
Unconformity
2nd Marine
cycle
Unconformity
1st Marine
cycle
Unconformity
NODEPOSITION
(? MINOR
REGRESSION
REGRESSION
(Continued
Transgression
Due to geoidal
Sea level rise)
TRANSGRESSION
(Geoidal sea level
Rise plus crustal
Movement)
Coal
Rank
~
~ ~
~
~
~ ~
~ ~
~ ~
~
~
~
~
~
~
~ ~
~
~ ~
~
~ ~
~ ~
~ ~
~ ~
~
~
~ ~
~~
~
~
~
~
~
~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~~ ~ ~
~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~
.
. .
. ..
... .
... .

4. Distribution of Possible Fatty Acids and Alkanones in some Thermally Immature Nigerian Coals
Uzoegbu et al. 106
MATERIALS AND METHODS
A total of nine samples comprising of six coals, two
carbonaceous shales and one coaly shale were collected
from 2 boreholes (BH94 and BH120) from Awgu Formation
(BH). The coal seams and interbedded shale in BH94 and
BH120 were sampled between 218-431 m and 131- 289
m depths respectively. In Mamu Formation, twelve
samples consisting of nine coals and three carbonaceous
shales were collected from Okaba (OBA) and Onyeama
(AMA) with co-ordinates of 07o 28ˈN, 07o 43ˈE and 06o 28ˈ
N, 07o 26ˈE).
In the laboratory, the samples were reshaped using a
rotating steel cutter to eliminate surface that could be
affected by alteration. Chips were cut from the samples
and dried in an oven at 105oC for 24 hours. The dried
sample was pulverized in a rotating disc mill to yield about
50 g of sample for analytical geochemistry. The samples
were subjected to flame ionization detection (FID) for
hydrocarbons thermal conductivity detection (TCD) for
CO2. One milligram of bulk powder sample was added to
200 mg of KBr and the mixture homogenized using a
pestle in an agate mortar. Pressing the mixture using a
load of 10 t yielded a pellet for Fourier Transform Infrared
(FT-IR) Spectroscopy using a Nicolet Bench 505P
Spectrometer, with sample absorbance monitored using
256 scans with resolution of 4 cm-1 from a wave-number of
4000 – 400 cm-1. About 10 g of the sample was subjected
to sohxlett extraction using a solvent mixture of acetone,
chloroform and methanol (47: 30: 23 v/v) at 60oC for 24
hours to extract the soluble organic matter. The extract
was concentrated by evaporation to dryness using a
rotating vapour evaporator at 250 mb. The extract was
transferred to an 8 ml vial using the same solvent mixture
and allowed to evaporate to dryness in a vented hood. The
dried extract was fractionated by silica gel column
chromatography with a column prepared using 2 g of baker
silica gel calcined at 200oC for 24 hours to yield six
fractions ranging from saturate to polar.
The saturate fraction was subjected to urea adduction to
separate isoprenoids from n-alkanes and subjected to gas
chromatography-mass spectrometry (GC-MS) using a CE
5980 GC coupled to an HP Finnigan 8222 MS held at 80oC
for three minutes and raised to 310oC at 3oC min-1 and held
isothermally for 10 minutes in order to assess some
molecular parameters used in source rock
characterization.
RESULTAND DISCUSSION
The distributions of fatty acids in the polar fraction have
been successfully used to differentiate the biological
source of geological materials (Duan et al., 1997).The m/z
58 and m/z 74 mass chromatograms showing the
distributions of the saturated n-fatty acids and alkan-2-
ones in the coal extracts are shown in Figs.3,4,5,6,7 and 8
respectively. Parameters calculated from the fatty acids
and alkanones distribution in the coal extracts are listed in
Tables 1 and 2 respectively.
Awgu samples have n-fatty acids ranging from C14 to C30,
maximizing at nC16 ornC18(Fig. 3). The short chain/long
chain saturated fatty acid (ATRFA) ratios for the samples
which range from 0.97-1.00, indicate both terrestrial and
marine organic matter derived material (Wilkes et al.,
1999). Abundance of short chain saturated n-fatty acids
(<nC20) in the samples reflects mixed input of
microorganisms and algae (Duan et al., 1997; Killops and
Killops, 2005). The nC16and nC18 are prominent in all the
samples. These compounds are ubiquitous and can also
reflect higher plant input e.g. seed and leaf oils of
gymnosperms (Volkman et al.,1998). The appreciable
amount of long chain saturated n-fatty acids(>C20) in the
samples can be attributed to curticular waxes of higher
plants (Cranwell,1974).
The carbon preference index (CPIFA) of the long chain n-
fatty acids (C24-C30) range between 1.98 and 3.29 (Table
1), indicating a strong even over odd predominance.
These values inferred high maturity status for the samples
(Wilkes et al., 1999). The distribution of straight chain n-
alkan-2-ones ranges from nC14 to nC33,maximizing at
nC17(Fig. 4). Similar distribution has previously been
observed in stalagmites (Xie et al., 2003; Bai et al., 2006).
However, some of the samples maximize at nC23 or
nC25(Fig. 4), an indication of contribution from higher
plants, microalgae and phytoplankton organic matter
inputs (Hernandez et al., 2001;Gonzalez-Vila et al., 2003).
Fig. 3: m/z 74 mass chromatogram showing the
distribution of n-fatty acids in Awgu samples (Numbers
refer to carbon chain lengths of n-fatty acids).
Fig. 3: (contd.): m/z 74 mass chromatogram showing the
distribution of n-fatty acids in Awgu samples (Numbers
refer to carbon chain lengths of n-fatty acids).

5. Distribution of Possible Fatty Acids and Alkanones in some Thermally Immature Nigerian Coals
Int. Res. J. Chem. Chem. Sci. 107
Table 1: Parameters calculated from n-Fatty acids and alkanones composition of Awgu Formation.
Sample N0 Depth (m) Lithology ATRFA CPILFA Pr-2-one/C17 CPI (alkanone)
BH218 218.5-222.5 Carbonaceous shale 0.99 nd 0.58 0.84
BH407 407.4-412.5 Coaly shale 0.99 nd 0.80 0.85
BH417 417.0-422.0 Coal 1.00 nd 1.09 1.14
BH131 131.7-136.6 Coal 0.99 nd 0.51 0.89
BH148 148 Coal 0.99 2.46 0.60 0.76
BH168 168.8-173.7 Coal 0.99 1.98 0.39 1.01
BH212 212.1-216.2 Coal 0.99 3.29 1.59 0.76
BH247 247 Carbonaceous shale 0.97 3.20 0.86 0.93
BH286 286.0-289.0 Coal 0.98 nd 0.82 1.20
ATRFA = Short chain/long chain saturated fatty acid
CPILFA= Carbon Preference Index (Longchain fatty acids)
CPI (alkanones)= Carbon Preference Index (alkan-2-ones).
ATRFA = C14 + C16 + C18 / C14 + C16 + C18 + C26 + C28 + C30
CPILFA=½{(C24+C26+C28+C30/C21+C23+C25+C27)+(C24+C26+C28+C30/C23+C25+C27+C29)}
CPI(alkanones)=1/2{(C25+C27+C29+C31+C33)/(C22+C24+C26+C28+C30+C32)
+(C25+C27+C29+C31+C33)/ C24+C26+C28+C30+C32+34}}
nd – Not determined
Fig. 4: m/z 58 mass chromatograms showing the
distributions of alkan-2-ones in Awgu samples (Numbers
refer to carbon chain lengths of alkan-2-ones).
Mamu samples have saturated n-fatty acids ranging from
C8 to C32 , maximizing at nC16 or nC18(Fig. 5 and 7). These
distributions reflect organic matter from both marine and
terrestrial materials (Volkman et al., 1998). However, the
dominance of short chain (<C20) saturated n-fatty acids
maximizing at C16 is an indication of substantial
contribution of microorganism/algal to the organic matter.
The appreciable quantity of long chain saturated n-fatty
acids (>nC22) in the samples canbe attributed to the
contribution of higher plants to the organic matter
(Cranwell, 1974). The short chain/long chain saturated
fatty acid (ATRFA) ratios range from 0.85 to 0.96. These
values indicate organic matter derived from mixed origin
(Wilkes et al., 1999). The carbon preference index
(CPILFA)for the long chain saturated n-fatty acids range
between 1.25 and 2.78, indicating a slight even over odd
predominance (Table 2). These values indicate low
maturity(Wilkes et al., 1999).
The n-alkan-2-ones range from nC12 to nC33, maximizing
at nC17 or nC29 (Fig. 6 and 8). These distributions reflect
higher plants and algae inputs to the organic matter (Bai
et al., 2006). The CPI values range from 1.27 to 1.69 and
2.10 to2.66 in Onyeama and Okaba samples respectively
(Table 2). These values indicate low maturity status for all
the samples (Tuo et al., 2007).
Fig. 5: m/z 74 mass chromatogram showing the
distribution of n-fatty acids in Mamu samples (Okaba)
(Numbers refer to carbon chain lengths of n-fatty acids).
Fig. 6: m/z 58 mass chromatograms showing the
distributions of alkan-2-ones in Mamu samples (Okaba)
(Numbers refer to carbon chain lengths of alkan-2-ones).

6. Distribution of Possible Fatty Acids and Alkanones in some Thermally Immature Nigerian Coals
Uzoegbu et al. 108
Table 2: Parameters calculated from n-Fatty acids and alkanones composition of Mamu Formation.
Sample N0 Depth (m) Lithology ATRFA CPILFA Pr-2-one/C17 CPI (alkanone)
AMA5 4.6-5.8 Carbonaceous shale 0.95 1.47 4.39 1.27
AMA4 6.0-6.8 Coal 0.91 1.37 10.54 1.45
AMA3 6.8-7.3 Coal 0.92 1.61 8.69 1.51
AMA2 7.6-8.4 Coal 0.92 2.07 12.18 1.69
AMA1 8.4-8.8 Coal 0.96 1.25 7.45 1.30
AMA6 9.0-9.5 Carbonaceous shale 0.94 1.61 4.10 1.60
OBA4 16.5-17.6 Carbonaceous shale nd nd nd nd
OBA3 18.0-18.5 Coal 0.85 2.78 8.68 2.66
OBA2 18.6-18.9 Coal 0.93 1.37 7.69 2.25
OBA1 18.9-19.3 Coal 0.94 1.95 12.69 2.59
OBA5 19.3-19.6 Coal 0.96 1.44 13.71 2.49
OBA6 19.6-20.0 Coal 0.91 2.51 21.43 2.10
ATRFA = Short chain/long chain saturated fatty acid
CPILFA= Carbon Preference Index (Longchain fatty acids)
CPI (alkanones)= Carbon Preference Index (alkan-2-ones).
ATRFA = C14 + C16 + C18 / C14 + C16 + C18 + C26 + C28 + C30
CPILFA=½{(C24+C26+C28+C30/C21+C23+C25+C27)+(C24+C26+C28+C30/C23+C25+C27+C29)}
CPI(alkanones)=1/2{(C25+C27+C29+C31+C33)/(C22+C24+C26+C28+C30+C32)
+(C25+C27+C29+C31+C33)/ C24+C26+C28+C30+C32+34}}
nd – Not determined
Fig. 7: m/z 74 mass chromatogram showing the
distribution of n-fatty acids in Mamu samples (Onyeama)
(Numbers refer to carbon chain lengths of n-fatty acids).
Fig. 7: (contd.): m/z 74 mass chromatogram showing the
distribution of n-fatty acids in Mamu samples (Onyeama)
(Numbers refer to carbon chain lengths of n-fatty acids).
Fig. 8: m/z 58 mass chromatograms showing the
distributions of alkan-2-ones in Mamu samples (Onyeama)
(Numbers refer to carbon chain lengths of alkan-2-ones).
CONCLUSION
Coal and coaly organic matter samples were collected
from coal bearing measures of Lower and Middle Benue
Trough, Nigeria. These samples were subjected to Gas
Chromatography and Gas Chromatography-Mass
Spectrometry analyses. The distributions of fatty acids and
n-alkan-2-ones showed that Awgu samples were formed
from organic matter derived from both terrestrial and
marine organic matter while Mamu samples were derived
from terrestrial organic matter.

7. Distribution of Possible Fatty Acids and Alkanones in some Thermally Immature Nigerian Coals
Int. Res. J. Chem. Chem. Sci. 109
REFERENCES
Adedosu TA (2009). Aspects of Organic Geochemistry of
Nigerian Coal as a Potential Source-Rock of Petroleum.
Ph.d Thesis, University of Ibadan, pp. 103-120.
Akande SO, Ogunmoyero IB, Petersen HI, Nytoft HP
(2007). Source Rock Evaluation of Coals from the
Lower Maastrichtian Mamu Formation, SE Nigeria.
Journal of Petroleum Geology 30.4: 303-324.
Bai Y, Fang X, Wang Y, Kenig F, Miao Y, Wang Y (2006).
Distribution of aliphatic ketones in Chinese soils:
Potential environmental implications. Organic
Geochemistry 37:860-869.
Barthlot W, Neinhuis C, Cutler D, Ditsch F, Meusel I,
Theisen I, Wilhelmi H (1998). Classification and
terminology of plant epicuticular waxes.
BotanicalJournal of the Linnean Society 126:237-260.
Bechtel A, Gruber W, Sachsenhofer RF, Gratzer R,
Püttmann W (2001). Organic geochemical and stable
carbon isotopic investigations of coals formed in low-
lying and raised mires within the Eastern Alps (Austria).
Organic geochemistry 32:1289-1310.
Brassell SC, Eglinton G, Marlowe IT, Pflaumann U,
Sarnthein M (1986). Molecular stratigraphy: a new tool
for climatic assessment. Nature 320:129-133.
Bray EE, Evans ED (1961). Distribution of n-paraffins as a
clue to recognition of source beds. Geochimica et
Cosmochimica Acta 22:2-15.
Brown FS, Baedeckner MJ, Nissenbaum A, Kaplan IR
(1972). Early diagenesis in a reducing fjord, Saanich
Inlet, British Coloumbia-III.Changes of inorganic
constituents of sediments. Geochimica et
Cosmochimica Acta 36:1185-1203.
Cranwell PA (1974). Monocarboxylic acids in lake
sediments: Indicators, derived from terrestrial and
aquatic biota of paleoenvironmental trophic levels.
ChemicalGeology 14:1-4.
Cranwell PA (1977). Organic geochemistry of Cam Loch
(Sutherland) sediments. Chemical Geology 20:205-
221.
Cranwell PA (1984). Lipid geochemistry of sediments from
Uptan Broad, a small productive lake. Organic
Geochemistry 7:25-37.
Cranwell PA, Eglinton G, Robinson N (1987). Lipids of
aquatic organisms as potential contributors to
lacustrine sediments. Organic Geochemisry 11:513-
527.
Duan Y, Song JM, Cui MZ, Luo BJ (1998). Organic
geochemical studies of sinking particulate material in
China Sea area In: organic matter influxes and
distributional features of hydrocarbon compounds and
fatty acids. Science inChina 41:208-214.
Duan Y, Wen QB, Zheng G, Luo BJ, Ma L (1997). Isotopic
composition and probable origin of individual fatty acids
in modern sediments from Ruoergai Marsh and Nansha
Sea, China. Organic Geochemistry 27.7/8:583-589.
Gonzalez-villa FJ, Polvillo O, Boski T, Moura D, de Andres
JR (2003). Biomarker patterns in a time-resolved
Holocene/terminal Pleistocene sedimentary sequence
from the Guadiana river estuarine area (SW
Portugal/Spain border). Organic Geochemistry
34:1601-1613.Bulletin 79:929-959.
Hernandez ME, Mead R, Peralba MC, Jaffe R (2001).
Origin and transport of n-alkan-2-ones in a subtropical
estuary: potential biomarkers for sea grass derived
organic matter. Organic Geochemistry 32:21-32.
Huang Y, Lockheart MJ, Collister JW, Eglinton G (1995).
Molecular and isotopic biogeochemistry of the Miocene
clarkia Formation: hydrocarbons and alcohols. Organic
Geochemistry 23:785-801.
Huang Y, Lockheart MJ, Logan GA, Eglinton G (1996).
Isotope and Molecular evidence for the diverse origins
of carboxylic acids in leaf fossils and sediments from
the Miocene Lake clarkia deposit, Idaho, USA.
OrganicGeochemistry 24:289-299.
Huang Y, Street-Perrott FA, Perrott RA, Metzger P,
Eglinton G (1999). Glacial/interglacial environmental
changes inferred from molecular and compound-
specific analyses of sediments from Sacred Lake, Mt.
Kenya.Geochimica et Cosmochimica Acta 63:1383-
1404.
Killops SD, Killops VJ (2005). Introduction to organic
geochemistry. Second edition. U.K: Blackwell
Publishing Limited.
Kogel-Knabner I (2002). The macromolecular organic
composition of plant and microbial residues as inputs to
soil organic matter. Soil Biology &Biochemistry 34:139-
162.
Lehtonen K, Ketola M (1990). Occurrence of long chain
acyclic methyl ketones in sphagnum and carex peats of
various degrees of humification. OrganicGeochemistry
15:275-280.
Leif RN, Simoneit BRT (1995). Ketones in hydrothermal
petroleums and sediments extracts from Guaymas
Basin, Gulf of Califonia.OrganicGeochemistry 23:889-
904.
Lockheart MJ, van Bergen PF, Evershed RP (2000).
Chemotaxonomic classification of fossil leaves from the
Miocene Clarkia lake deposit, Idaho, USA based on n-
alkyl lipid distributions and principal component
analyses. Organic Geochemistry 31:1223-1246.
Logan GA, Eglinton G (1994). Biogeochemistry of the
Miocene lacustrine deposit at Clarkia, nothern Idaho,
USA. Organic Geochemistry 21:857-870.
Mbulk LN, Rao VR, Kumarn KPN (1985). The Upper
Cretaceous -Paleocence boundary in the Ohafia-Ozu
Abarn area, Irno State, Nigeria. Jour. Min. Geol., 22,
105-113.
Murat RC (1972). Stratigraphy and paleogeography of the
Cretaceous and lower Tertiary in southern Nigeria. In:
African Geology, T. F. J. Dessauvagie and A. J.
Whiteman, Ed. Ibadan University press, Ibadan,
Nigeria, p. 251-266.
Otto A, Simpson MJ (2006). Sources and composition of
hydrolysable aliphatic lipids and phenols in soils from
western Canada. Organic Geochemistry 37:385-407.
Phral FG, Wakeham SG (1987). Calibration of
unsaturation patterns in long chain ketone

8. Distribution of Possible Fatty Acids and Alkanones in some Thermally Immature Nigerian Coals
Uzoegbu et al. 110
compositions for palaeotemperature assessment.
Nature 330: 367-369.
Püttmann W, Bracke R (1995). Extractable organic
compounds in the clay mineral sealing of a waste
disposal site. Organic Geochemistry 23:43-54.
Reyment RA (1965). Aspects of the geology of Nigeria.
Ibadan. Univ. Press, Ibadan, Nigeria, 1965, p.145.
Rieley G, Collier RJ, Jones DM, Eglinton G (1991). The
biogeochemistry of Ellesmere Lake, UK-I: source
correlation of leaf wax inputs to the sedimentary lipid
record. Organic Geochemistry 17:901-912.
Rontani JF, Giral RJP, Baillte G, Raphel D (1992). ”Bound”
6,10,14- trimethylpentadecan-2-one: a useful marker
for photo degradation of chlorophylls with a phytol ester
group in sea water. Organic Geochemistry 18:139-142.
Schouten S, Hoef, MJL, Sinninghe Damste JS (2000). A
molecular and stable carbon isotopic study of lipids in
late Quartenary sediments from the Arabian Sea.
Organic Geochemistry 31:509-521.
Simoneit BRT (1998). Biomarker PAHs in the
environment. In: Neilson, A., Hutzinger, O., editors. The
handbook of environmental chemistry. Berlin: Springer
Verlag. 175-221.
Simoneit BRT, Cox RE, Standley LJ (1988). Organic
matter of the troposphere-IV: lipids in harmattan
aerosols of Nigeria. AtmosphericEnvironment 22:983-
1004.
Simoneit BRT, Sheng GY, Chen XJ, Fu JM, Zhang J, Xu
YP (1991). Molecular marker study of extractable
organic matter in aerosols from urban areas of China.
Atmospheric Environment 25A: 2111-2129.
Simpson A (1955). The Nigeria coalfield. The geology of
parts of Onitsha, Owerri and Benue provinces. Bull.
Geol. Sur. Nigeria, 24, 1-85.
Sonzogoni C, Bard E, Rostek F, Dollfus D, Roselle-Melle
A, Eglinton G (1997). Temperature and salinity effects
on the alkenone ratios measured in surface sediments
from the Indian ocean. Quartenary Research 47:344-
355.
Tattam CM (1944). A review of Nigerian stratigraphy.
Annual report, Geol. Sur. Nig., 1943, 27-46.
Tuo J, Li Q (2005). Occurrence and distribution of long-
chain acyclic ketones in immature coals. Applied
Geochemistry 20:553-568.
Tuo J, Ma W, Zhang M, Wang X (2007). Organic
geochemistry of the Dongsheng sedimentary uranium
ore deposits, China. Applied Geochemstry 22:1949-
1969.
Uzoegbu UM, Uchebo UA, Okafor I (2013). “Petroleum
generation potential of late Cretaceous coals from the
Anambra Basin, SE Nigeria.” Nig. J. Manpower Dev.
Change, vol. 1 no.1, p. 102-120, 2013.
Volkman JK, Barret SM, Blackburn SI, Sikes EL (1995).
Alkenones in Gephyrocapsa oceanica: implications for
studies of paleoclimate. Geochimicaet Cosmochimica
Acta 59:513-520.
Volkman JK, Barrett SM, Blackburn SI, Mansour MP,
Sikes EL, Gelin F (1998). Microalgal biomarkers: a
review of recent research developments. Organic
Geochemistry 29:1163-1179.
Volkman JK, Farrington JW, Gagosian RB, Wakeham SG
(1983). Lipid composition of coastal marine sediments
from the Peru upwelling region. InAdvances in Organic
Geochemistry, 1981,eds.M.Bjoroy et.al. Chichester:
Wiley. 228-240.
Volkman JK, Johnson RB, Gillian FT, Perry GT, Bavor HJ
(1980). Microbial lipids of intertidal sediment-I. Fatty
acids and hydrocarbons. Geochimica et Cosmochimica
Acta 44:1133-1143.
Wilkes H, Ramrath A, Negendank JFW (1999). Organic
geochemical evidence for environmental changes
since 34,000 yrs BP from Lago di Mezzano, central
Italy. Journal of Paleolimnology 22:349–365.
Xie S, Yi Y, Huang J, Hu C, Cai Y., Collins M, Baker A
(2003c). Lipid distribution in a subtropical southern
China stalagmite as a record of soil ecosystem
response to palaeoclimatic change. Quaternary
Research 60: 340-347.
Yuang H, Huang Y (2003). Preservation of lipid hydrogen
isotope ratios in Miocene lacustrine sediments and
fossils at Clarkia, northern Idaho, USA. Organic
Geochemistry 34:413-423.
Accepted 26 July 2019
Citation: Uzoegbu M.U., Oghonyon R., Ugwueze C.U
(2019). Distribution of Possible Fatty Acids and Alkanones
in some Thermally Immature Nigerian Coals. International
Research Journal of Chemistry and Chemical Sciences
6(1): 103-110.
Copyright: © 2019. Uzoegbu et al. This is an open-access
article distributed under the terms of the Creative
Commons Attribution License, which permits unrestricted
use, distribution, and reproduction in any medium,
provided the original author and source are cited.