GEOLOGICA CARPATHICA, 53, 2, BRATISLAVA, APRIL 2002
103 — 108
PALEOZOIC CLAYS OF TUNISIA
FAKHER JAMOUSSI
1
, SAMIR KHARBACHI
2
, FERNANDO ROCHA
3
, ALBERTO LOPEZ GALINDO
4
,
CELSO GOMES
3
, JOELLE DUPLAY
5
, RABAH ALOUANI
6
and FOUAD ZARGOUNI
7
1
Laboratoire Géoressource, INRST BP 95, 2050 Hamam-lif, Tunisia; Fakher.Jamoussi@inrst.rnrt.tn
2
SEREPT, 8 Rue Slimen Ben Slimen Manar II Tunis, Tunisia
3
Univ. Aveiro, Campo de Santiago, 3810 Aveiro, Portugal; frocha@geo.ua.pt, cgomes@geo.ua.pt
4
Facultad de Sciencias, Fuentenueva S/N, 18002-Grenada, Spain; Alberto@goliat.ugr.es
5
Centre de géochimie de surface, 1 rue Blessig, F-67200 Strasbourg, France
6
Département de Géologie, Fac. des Sc. de Bizerte, 7021 Zarzouna, Bizerte, Tunisia
7
Département de Géologie, Faculté des Sciences de Tunis, 1060 Belvédère, Tunis, Tunisia
(Manuscript received October 4, 2001; accepted in revised form December 13, 2001)
Abstract: The oil drilling holes carried out on the Saharan Platform (southern Tunisia) produced evidence of the pres-
ence of Paleozoic bedrock. The dominant lithology of the Lower Paleozoic is clays and sandstones whereas the Upper
Paleozoic is marked by carbonated sandstone and clayey marine series. The qualitative and semiquantitative mineralogi-
cal compositions (bulk rock and clay fraction) were evaluated by X-ray diffraction, using Siemens Kristalloflex 810
diffractometer. The chemical analyses of major elements were carried out by Atomic Absorption Spectrophotometry.
Trace and rare earth elements were determined by ICP-MS Perkin-Elmer SCIEX Elan-5000. Chemical microcomposition
was determined using Phillips CM20 STEM. The mineralogical studies of Paleozoic clays showed the predominance of
illite accompanied by small amounts of kaolinite and chlorite. The geochemical data put in evidence the relatively high
amounts of Fe
2
O
3
and Na
2
O which are most probably associated with aluminosilicates. The flat pace of the rare earth
curve analyzed in relation to the NASC indicates the tendency to the impoverishment in HREE.
Key words: Paleozoic, Tunisia, geochemistry, mineralogy, clays.
Introduction
The studied region is located close to the southern border of Tu-
nisia corresponding to the Saharan Platform domain (Fig. 1).
The Precambrian bedrock is covered by Paleozoic sub-tabu-
lar clay and sand series, which have been sealed unconform-
ably by a Mesozoic succession of strata (Berkaloff 1933;
Bonefous 1963; Busson 1967; Memmi et al. 1986; Bouaziz
1995). The Paleozoic series related to the oil drilling in the
south of Tunisia were studied from the mineralogical and
geochemical point of view.
Geological setting
Precambrian and Paleozoic formations do not outcrop on the
surface in Tunisia. The only exception is the Permian deposit
outcropping close to Djebel Tebaga, west of Medenine. How-
ever, the oil drilling works carried out in the South of Tunisia
crossed the different periods of the Paleozoic (Memmi et al.
1986; Ben Ferjani et al. 1990).
The Cambrian is represented by a thick set of sandstone as-
signed to the Sidi Toui Formation. This unit rests in discor-
dance on the crystalline and metamorphic bedrock (Memmi et
al. 1986).
The series assigned to the Ordovician consist essentially of
clay and sandstone in the basis, evolving to a clay-conglomer-
atic series in the top (Memmi et al. 1986; Jamoussi 2001).
The Silurian starts with an essentially clayey sequence, ra-
dioactive and rich in organic matter. It has been assigned to the
Tannezouft Formation. The succession becomes enriched it-
self in sandstone components forming the Acacus Formation
(Jeager et al. 1995).
The Devonian is found in the south of the Dahar arc. The
Devonian marks the return to deposits of clay and sandstone.
The Carboniferous brought a return to more straightforward-
ly marine conditions. It is found in the Southern border of Tu-
nisia and NE of the Saharan Platform, represented by clay,
limestone and sandstone.
The Permian occurs only in the North of the Saharan Plat-
form, in the furrow of the Jeffara where it can reach some im-
portant thickness. The Permian of the Tebaga Formation, of
which only the top section outcrops in the Northwest of Mede-
nine, constitutes the only African outcrop of marine Permian
represented by bioclastic limestone, argillaceous limestone
and clay (Khessibi 1985).
Permo-Triassic deposits of the Haïrech, located in the
Northern Atlas, were studied for comparison. They are formed
by a thick formation of slightly metamorphized, pelitic sand-
stone. It is a regular sequence of thin sandstone and clay in
thin beds (Alouani & Tlig 1988).
Materials and methods
Several samples of drill cores BMT1 and LG2 (see Fig. 1
for location), were studied as representatives of the different
Paleozoic formations.
The qualitative and semiquantitative mineralogical compo-
sitions (bulk rock and clay fraction) were evaluated by X-ray
MECC ‘01
104 JAMOUSSI et al.
diffraction, using a Siemens Kristalloflex 810 diffractometer,
Cu-K
α
radiation, by the powder method (bulk rock) and as
oriented preparations (clay fraction), air-dried, saturated with
ethylene glycol and heated to 550
°C.
Quantification of different phases was carried out by the
classic method of diffraction peak area measurement and re-
flection power (Millot 1964; Schultz 1964; Biscaye 1965;
Barahona 1974; Mellinger 1979; Brindley & Brown 1980;
Caillere et al. 1982; Pevear & Mumpton 1989).
The chemical analyses of major elements were carried out
by Atomic Absorption Spectrophotometry. Trace and rare
earth elements were determined by a ICP-MS Perkin-Elmer
SCIEX Elan-5000, using Rh and Re as internal standards. Ac-
curacy was 2% and 5% for 50 ppm and 5 ppm, respectively.
The detection limits of elements were 100 ppb for REE and
Th, 5 ppm for transition elements and Cs, Rb, Sr, Ba and Pb,
and 10 ppm for Li. Chemical microcomposition was deter-
mined using a Phillips CM20 STEM.
Results and discussion
The mineralogical studies of Paleozoic clays showed the
general predominance of siliciclastic minerals in the bulk-rock
compositions and of illite in their clay fractions (Fig. 2 and Ta-
ble 1).
Analysis of the mean values of the bulk-rock mineralogical
composition for each one of the stratigraphic units revealed an
almost regular alternation of phyllosilicate rich units with
units rich in quartz. Only the Lower Permian and Upper Car-
boniferous are enriched in carbonate minerals (mainly dolo-
mite).
The clay fractions show (Fig. 2 and Table 1) the general pre-
dominance of illite associated with kaolinite and chlorite. Up-
per Carboniferous, Lower and Upper Silurian formations are
the only exceptions to this rule.
Clay mineral association (illite + kaolinite + chlorite) char-
acterizes the Cambrian-Ordovician and Lower Ordovician pe-
Fig. 2. XRD patterns of Carboniferous clay.
Fig. 1. Location of the studied zone.
PALEOZOIC CLAYS OF TUNISIA 105
riod. Chlorite is of Fe-type and, according to Giblin & Cahen
(1982) and Jamoussi (2001), essentially authigenic. These de-
trital siliciclastic deposits evolve from finer ones at the base to
coarser ones (conglomeratic) towards the top. This sedimento-
logical evolution is also recorded in the mineralogical compo-
sition by the enrichment in quartz (bulk-rock) and in illite (clay
fraction), as well as by the impoverishment in feldspars and
chlorites. These deposits have been considered to be perigla-
cial marine sediments, low energetic at the base and high ener-
getic at the top.
Silurian (Upper and Lower) deposits are finer and richer in
phyllosilicates, presenting the enrichment in kaolinite, associ-
ated with illite and chlorite, the latter being essentially authi-
genic, increasing from the Lower Silurian to the Upper Siluri-
an. This mineralogical signature points out to environmental
changes occurring in the Lower Silurian, more favourable to
chemical alteration and transformation, vanishing during the
Upper Silurian.
Clays of the Devonian show again a clear predominance of
illite with little kaolinite and chlorite (Jamoussi 2001), the de-
posits being essentially the product of fresh detrital continental
supplies.
From the Lower Carboniferous to the Upper Carboniferous
the strong increase in dolomite (bulk-rock) and in kaolinite
(clay fraction) contents is counterbalanced by the decrease in
quartz, illite and chlorite contents. These carbonate deposits
are clearly marine, brackish, deposited in relatively confined
waters.
The Permian shows again a predominance of illite accom-
panied by kaolinite and also, in Upper Permian, by chlorite; in
some Permian outcrops smectite and illite-smectite are
present, decreasing then the relative illite and chlorite contents
(Table 1). These deposits are mainly continental with lagoonal
episodes, presenting some marine domains (carbonate plat-
forms, reefs), the sediments having not been submitted to sub-
stantial pressure and temperature increases.
The chemical analyses of the major elements (Table 2) were
performed only in the bulk-rock samples. It can be noticed
that Al
2
O
3
presents a strong interrelationship with Fe
2
O
3
(r =
0.64 correlation factor) and Na
2
O (r = 0.62), which confirms
that these elements are contained in aluminosilicate minerals.
On the other hand, Al
2
O
3
content presents a very weak inter-
relationship with K
2
O (r = 0.03).
Trace element contents (Tables 3a and 3b; Fig. 3) show a
regular behaviour for five analyzed stratigraphic intervals:
Cambrian-Ordovician, Lower Devonian, Upper Permian, Per-
mian and Permo-Triassic, the latter showing a slight impover-
ishment in relation to the others (see SP5 at Fig. 3).
Rare earth element (REE) contents (Table 4) are plotted af-
ter NASC normalization (Fig. 4), showing a practically flat
Table 1: Mineralogical composition of the studied Paleozoic sequences of the Saharan Platform. (Phyll – phyllosilicate, Ca – calcite, Dol
– dolomite, Qz – quartz, Gyp – gypsum, Feld – feldspar, Sm – smectite, Ill – illite, Kaol – kaolinite, Ill/Sm – interstratified illite
smectite, Chl – chlorite.)
Stratigraphic unit
Bulk-rock Mineralogy
Clay-fraction Mineralogy
Phyll
Ca
Dol
Qz
Gyp
Feld
Sm
Ill
Kaol
Ill/Sm
Chl
Permo-Triassic - Hirech
57
0
0
36
0
7
0
97
3
0
0
Permian - Dkilet Toujan
81
5
0
8
5
2
11
45
18
21
6
Upper Permian
59
4
8
26
0
3
0
75
14
0
11
Lower Permian
20
0
74
5
0
1
0
83
17
0
0
Upper Carboniferous
38
0
30
31
0
1
0
36
55
0
9
Lower Carboniferous
50
0
0
45
0
5
0
75
14
0
11
Upper Devonian
55
0
0
38
0
7
0
77
13
0
10
Lower Devonian
45
1
1
52
0
1
0
80
12
0
8
Upper Silurian
51
1
0
44
0
4
0
37
45
0
18
Lower Silurian
58
1
0
39
0
2
0
42
49
0
9
Lower Ordovician
23
1
1
70
0
5
0
80
12
0
8
Cambrian-Ordovician
34
1
1
46
0
18
0
77
13
0
10
Table 2: Chemical composition (major elements in %) of the studied Paleozoic sequences of the Saharan Platform.
Stratigraphic unit
SiO
2
Al
2
O
3
Fe
2
O
3
CaO
MgO
Na
2
O
K
2
O
SO
=
3
IL
SiO
2
/Al
2
O
3
Fe
2
O
3
/Al
2
O
3
Al
2
O
3
/K
2
O
Permo-Triassic - Hirech
72.91
12.68
4.14
0.18
0.34
0.54
4.22
2.76
5.75
0.33
3.00
Permian - Dkilet Toujan
42.50
17.44
8.65
6.44
2.28
0.50
3.86
3.56
14.42
2.44
0.50
4.52
Upper Permian
47.14
16.58
5.92
4.93
3.53
1.17
3.60
2.51
13.34
2.84
0.36
4.61
Lower Permian
15.40
7.90
3.43
20.16
14.59
0.15
1.88
0.00
34.76
1.95
0.43
4.20
Upper Carboniferous
46.29
16.98
5.57
7.14
4.97
0.16
3.69
3.59
10.49
2.73
0.33
4.60
Lower Carboniferous
49.42
20.04
6.15
6.31
2.58
1.40
5.78
1.65
6.48
2.47
0.31
3.47
Upper Devonian
50.93
22.67
7.72
0.35
1.58
1.19
2.58
0.65
11.69
2.25
0.34
8.79
Lower Devonian
55.34
20.78
6.00
2.25
1.11
0.84
2.77
1.06
9.15
2.66
0.29
7.50
Upper Silurian
50.85
20.42
11.44
0.71
1.63
1.46
2.53
0.74
10.18
2.49
0.56
8.07
Lower Silurian
50.99
21.73
9.58
0.50
1.14
1.79
2.41
0.79
10.48
2.35
0.44
9.02
Lower Ordovician
57.13
17.85
5.38
3.29
1.54
0.62
4.82
1.21
8.05
3.20
0.30
3.70
Cambrian-Ordovician
61.98
18.72
5.58
0.17
1.28
0.88
5.78
0.00
3.26
3.31
0.30
3.24
106 JAMOUSSI et al.
tendency of lines, but putting in evidence of some impoverish-
ment in heavy rare earth elements (HREE), in particular for
the Permo-Triassic (SP5).
Table 5 shows the structural formulas of clay minerals from
some of different studied stratigraphic formations. These
structural formulas were computed supposing that all chemical
charges are compensated. For illite, iron is regarded as triva-
lent, for chlorites as divalent.
Structural formula of one of the Ordovician illites:
K
0.75
Mg
0.05
(Al
1.73
Mg
0.11
Fe
3+
0.20
) (Si
3.16
Al
0.84
) O
10
OH
2
Structural formula of one of the Silurian illites:
K
0.82
(Al
1.63
Mg
0.23
Fe
3+
0.21
) (Si
3.21
Al
0.79
) O
10
OH
2
a
Stratigraphic unit
Sample
Li
Rb
Cs
Be
Sr
Ba
Sc
V
Cr
Co
Ni
Cu
Zn
Permo-Triassic Hirech
SP5
5.3
108.2
3.7
2.2
13.8
253.1
12.1
91.5
150.4
1.4
34.9
2.3
1.7
Permian Dk. Toujane
Pr1
54.0
151.1
8.1
3.1
272.0
190.1
22.2
164.8
149.6
10.7
66.4
13.6
65.1
Upper Permian
PRM3
118.2
217.2
17.9
2.6
167.4
191.3
18.6
200.5
148.8
6.4
42.8
14.5
48.7
Lower Devonian
DV2
111.0
129.1
10.9
2.9
65.4
137.9
20.2
151.1
129.5
12.0
54.9
26.6
65.2
Cambrian-Ordovician
ORD1
34.5
330.0
19.4
3.6
34.5
316.0
17.3
114.6
134.6
5.8
24.0
7.6
43.8
b
Stratigraphic unit
Sample
Ga
Y
Nb
Ta
Zr
Hf
Mo
Sn
Tl
Pb
U
Th
Permo-Triassic Hirech
SP5
17.7
4.2
2.6
0.2
2.2
0.1
0.5
4.1
0.3
2.4
0.7
7.0
Permian Dk. Toujane
Pr1
28.4
18.2
13.8
1.0
103.9
3.1
2.0
7.2
0.7
18.4
2.4
14.4
Upper Permian
PRM3
35.9
10.5
9.8
0.7
89.9
2.8
2.2
94.2
1.0
12.5
1.9
10.1
Lower Devonian
DV2
35.5
15.4
10.5
1.3
51.5
1.7
2.0
39.9
0.8
27.8
1.5
17.8
Cambrian-Ordovician
ORD1
35.2
10.1
12.9
1.5
34.9
1.4
2.0
80.5
1.4
11.2
4.0
19.8
Sample
La
Ce
Pr
Nd
Sm
Eu
Gd
Tb
Dy
Ho
Er
Tm
Yb
Lu
SP5
27.55
62.48
7.31
27.97
5.26
1.03
2.83
0.31
1.06
0.17
0.36
0.05
0.30
0.04
Pr1
45.45
93.38
10.92
40.80
7.55
1.47
5.63
0.78
3.98
0.74
2.00
0.28
1.86
0.28
PRM3
21.36
42.34
4.61
15.83
2.27
0.41
1.49
0.28
1.86
0.43
1.26
0.21
1.34
0.23
DV2
38.55
79.76
8.17
27.10
4.45
0.89
3.15
0.47
2.76
0.59
1.66
0.27
1.75
0.27
ORD1
26.76
55.24
5.93
19.37
3.38
0.61
1.94
0.31
1.83
0.39
1.15
0.18
1.10
0.17
Table 4: Chemical composition (rare earth elements in ppm) of the studied Paleozoic sequences of the Saharan Platform.
Table 3a,b: Chemical composition (trace elements in ppm) of the studied Paleozoic sequences of the Saharan Platform.
Fig. 3. Trace element distribution curves.
Fig. 4. Rare earth element distribution curves (NASC – normalized).
Structural formula of one of the Silurian paragonites:
K
0.35
Na
0.18
Mg
0.09
(Al
1.81
Fe
3+
0.29
) (Si
2.99
Al
1.01
) O
10
OH
2
Structural formula of one of the Permian chlorites:
K
0.55
(Al
1.51
Mg
0.18
Fe
2+
2.25
Ti
0.05
) (Si
3.60
Al
0.40
) O
10
OH
8
Structural formula of one of the Permo-Triassic illites:
K
0.72
Mg
0.01
(Al
1.53
Mg
0.37
Fe
3+
0.18
Ti
0.01
) (Si
3.30
Al
0.70
) O
10
OH
2
The studied samples of the Tunisian Paleozoic present illites
showing irregular degrees of crystallinity, as can be seen from
Figure 5. The majority of the analyzed samples shows Kubler
Crystallinity Index for illite corresponding to medium up to
well ordered values which are located in the zone of diagene-
PALEOZOIC CLAYS OF TUNISIA 107
Samples
Tetrahedral sheet
Octahedral sheet
Interlayer cations
Si
Al
IV
Al
VI
Mg
Fe
Ti
K
Ca
Na
Mg
Ord1/1 illite
3.11
0.89
1.61
0.18
0.27
0.00
0.87
0.00
0.00
0.01
Ord1/2 illite
3.21
0.79
1.85
0.04
0.12
0.00
0.64
0.00
0.00
0.08
Mean ORD1 illite
3.16
0.84
1.73
0.11
0.20
0.00
0.75
0.00
0.00
0.05
SLR2/2 illite
3.21
0.79
1.63
0.23
0.21
0.00
0.82
0.00
0.00
0.00
SLR2/3 illite-paragonite
2.99
1.01
1.81
0.00
0.29
0.00
0.35
0.00
0.18
0.09
Pr1/2 chlorite
3.60
0.40
1.51
0.18
2.25
0.05
0.55
0.00
0.00
0.00
SP5/1 illite
3.27
0.73
1.46
0.45
0.21
0.01
0.76
0.00
0.00
0.00
SP5/2 illite
3.38
0.62
1.50
0.44
0.16
0.01
0.72
0.00
0.00
0.00
SP5/3 illite
3.25
0.75
1.64
0.23
0.19
0.02
0.67
0.00
0.00
0.04
Mean SP5 illite
3.30
0.70
1.53
0.37
0.18
0.01
0.72
0.00
0.00
0.01
Stratigraphic units
Bulk-rock phases
Clay-fraction
Paleoambiental interpretations
Permian- Dkilet Toujan
Phyll, Qz, Ca
Ill, Sm/Ill-Sm, Kaol
Continental, lagoonal episodes
Upper Permian
Phyll, Qz, Dol
Ill, Kaol, Chl
Marine, deep sea
Lower Permian
Dol, Phyll
Ill, Kaol
Carbonated platforms, reef
Upper Carboniferous
Phyll, Qz, Dol
Kaol, Ill, Chl
Marine, brackish, confined
Lower Carboniferous
Phyll, Qz, Feld
Ill, Kaol, Chl
Transition environment
Upper Devonian
Phyll, Qz, Feld
Ill, Kaol, Chl
Decrease of the detrital supply
Lower Devonian
Qz, Phyll
Ill, Kaol, Chl
Fresh detrital continental supply
Upper Silurian
Phyll, Qz
Kaol, Ill, Chl
Vanishing of chemical alteration
Lower Silurian
Phyll, Qz
Kaol, Ill, (Chl)
Increase of chemical alteration
Lower Ordovician
Qz, Phyll, (Feld)
Ill, Kaol, Chl
Periglacial marine, high energetic
Cambrian-Ordovician
Qz, Phyll, Feld
Ill, Kaol, Chl
Periglacial marine, low energetic
Table 6: Non clay minerals and clay minerals assemblages of the Tunisian Paleozoic clayey units, and paleoambiental interpretations.
(Phyll – phyllosilicate, Ca – calcite, Dol – dolomite, Qz – quartz, Gyp – gypsum, Feld – feldspar, Sm – smectite, Ill – illite, Kaol
– kaolinite, Ill/Sm – interstratified illite smectite, Chl – chlorite).
Table 5: Numbers of ions in crystal structure formulas of clay minerals from the studied stratigraphic formations.
sis but coming closer to the anchizone (Fig. 5). The only sam-
ple plotted clearly in the epizone belongs to the Permo-Trias-
sic of Hirech confirming the sudden metamorphism presented
by these levels.
A synthesis of the mineralogical characterization of Tuni-
sian Paleozoic clayey units is shown in Table 6, as well as the
proposal of some paleoenvironmental inerpretations.
Conclusions
Paleozoic clays from Tunisia sampled in oil drill cores were
studied. The mineralogy of these clays shows a predominance
of well crystallized illite accompanied by smaller contents of
kaolinite and chlorite. Fe
2
O
3
and Na
2
O contents are essentially
concentrated in aluminosilicates. The rare earth element repre-
sentation in relation to the NASC, shows the practically flat
curves and the tendency to the impoverishment in heavy rare
earth elements.
Clayey Paleozoic sediments are produced from the alter-
ation of the crystalline basement and subsequently influenced
by diagenetic transformation. The higher illite crystallinity
shown in certain strata indicates on the one hand the diagene-
sis action and on the other hand the influence of diverse oro-
geneses rejuvenated the relief consequently favouring the
transport of detrital materials. Clay mineral assemblages re-
flect the climatic oscillations as well as the effects of tectonic
events.
References
Alouani R. & Tlig S. 1988: Métamorphisme et dolomitisations suc-
cessives dans deux mégaséquences superposées au jebel
Haïrech (Tunisie Nord occidentale). C.R. Acad. Sci. Paris 306
II, 1373—1378.
Barahona E. 1974: Argcillas de ladrilleria de la provencia de Grana-
da: evalucion de algunos ensayos de materias primas. Tesis
Doctoral, Secret. Public. Univ. Granada, 1—398.
Ben Ferjani A., Burollet P.F. & Mejri F. 1990: Petroleum geology of
Tunisia. Revue Etap. 1—194.
Berkaloff E., Douvillé H. & Solignac M. 1933: Découverte du Per-
mien du Djebel Tebaga. C.R. Acad. Sci. Paris 196 n°1, 21—24.
Biscaye P.E. 1965: Mineralogy and sedimentation of recent deep-
Fig. 5. Illite crystallinity (Kubler index vs. Esquevin index).
108 JAMOUSSI et al.
sea clay in the Atlantic Ocean and adjacent seas and ocean.
Geol. Soc. Am. Bull. 76, 803—832.
Bonefous J. 1963: Synthèse stratigraphique sur le Gothlandien des
sondages du Sud Tunisien. R. Inst. Franç. Pétrole. Paris 18,
10, 1434—1447.
Bouaziz S. 1995: Etude de la tectonique cassante dans la plate-
forme et l’Atlas saharien (Tunisie méridionale): évolution des
paléochamps de contraintes et implications géodynamiques.
Th
èse es Science, Fac. SC. Tunis. Univ. Tunis II. 1—485.
Brindley G.W. & Brown 1980: Crystal structure of clay minerals
and their X-Ray identification. Mineralogical Society. Mono-
graph n°5. 1—495.
Busson G. 1967: Le Mésozoïque Saharien. 1
čre
partie: Extrême Sud
tunisien. CNRS, Paris, (Série Géologique) 8, 1—194.
Caillère S., Henin S. & Rautureau M. 1982: Minéralogie des argiles.
1: Structures et propriétés physico-chimiques. 2: Classification
et nomenclature. 2
čme
Edition, Masson, 1—189.
Giblin P. & Cahen H. 1982: Tunisie permis de Kirchaou. Résultats
de géochimie minérales. Geo/Lab. Pau. n°205/82 RP. Rapport
interne. SEREPT 18.
Jaeger H., Bonnefous J. & Massa D. 1975: Le silurien en Tunisie:
ses relations avec le silurien de Libye nord-occidentale. Bull.
Soc. Géol. Fr. Paris 17, 68—76.
Jamoussi F. 2001: Les argiles de Tunisie: étude minéralogique,
géochimique, géotechnique et utilisations industrielles. Thèse
Doctorat Es-Science. Univ. Tunis El Manar. Fac. Sc. Tunis, 1—
437.
Khessibi M. 1985: Etude sédimentologique des affleurements per-
miens du Djebel Tebaga de Mednine (Sud Tunisien). Bull. Cen-
tres Rech. Exlor. Prod. Elf-Aquitaine 9, 2, 427—464.
Mellinger R.M. 1979: Quantitative X-ray diffraction analysis of
clay minerals. An evaluation. SRC Rep. Saskatchewan Res.
Counc. G-79, 1—46.
Memmi L., Burollet P.F. & Viterbo I. 1986: Lexique stratigraphique
de la Tunisie. Première partie: Précambrien et paléozoïque.
Note du service géologique de Tunisie 53, 1—63.
Millot G. 1964: Géologie des argiles: Altération, sédimentologie,
géochimie. Ed. Masson et Cie, Paris, 1—499.
Pevear D.R. & Mumton D.R. 1989: Quantitative mineral analysis of
clays. CMS Workshop Lectures, 1. The Clay Mineral Society,
Colorado.
Schultz L.G. 1964: Quantitative interpretation of mineralogical
composition from X-ray and chemical data for the Pierre shale.
U.S. Geol. Surv. Profes. Paper 391—C, 1—31.