261
GRANITOID PEBBLES FROM OLIGOCENEMIOCENE DEPOSITS OF THE RIFIAN CHAIN (MOROCCO)
GEOLOGICA CARPATHICA, 55, 3, BRATISLAVA, JUNE 2004
261272
PETROGRAPHY AND GEOCHEMISTRY OF GRANITOID PEBBLES
FROM THE OLIGOCENE-MIOCENE DEPOSITS OF THE INTERNAL
RIFIAN CHAIN (MOROCCO): A POSSIBLE NEW HYPOTHESIS OF
PROVENANCE AND PALEOGEOGRAPHICAL IMPLICATIONS
LISA GIOCONDA GIGLIUTO
1
, ABDELOUAHED OUAZANI-TOUHAMI
2
, DIEGO PUGLISI
1
,
GIUSEPPA PUGLISI
1
and MOHAMED NAJIB ZAGHLOUL
3
1
Dipartimento di Scienze Geologiche, University of Catania, Corso Italia 55, 95129 Catania, Italy; geolisa@infinito.it;
dpuglisi@mbox.unict.it; gpuglis@mbox.unict.it
2
Département de Géologie, Faculté des Sciences, Université Abdelmalek Essaadi de Tétouan, Maroc; aouzani@fst.ac.ma
3
Département des Sciences de la Terre et dOcéanologie, Faculté des Sciences et Techniques, Université Abdelmalek Essaadi de Tanger,
Maroc; zaghloul@nirvanet.net
Corresponding autor: Diego Puglisi; Tel.: 0039-095-7195724; Fax: 0039-095-7195728; dpuglisi@mbox.unict.it
(Manuscript received April 29, 2003; accepted in revised form October 2, 2003)
Abstract: The Oligocene-Miocene deposits of the Internal Domains and of the innermost sectors of the flysch basin,
recognized along the Betic-Rifian Chain (Spain and Morocco; i.e. Malaguide/Ghomaride Units and maurétanien flysch,
respectively), are characterized by the occurrence of crystalline pebbles within several conglomerate horizons. Their
provenance is difficult to explain because of the absence of similar rocks in the pre-Alpine Paleozoic basement nappes of
this chain. Geochemical characters of seven granitoid pebbles (two-mica, cordierite-bearing monzogranite up to leuco-
monzogranite), sampled from conglomerate lithofacies occurring within the above mentioned sandstone suites (Internal
Rif and maurétanien sector of the flysch basin), have been determined and compared with other plutonic rocks of the
Western Mediterranean and Iberian areas in order to detect their provenance. This comparison has been realized with the
syn- to late-Hercynian plutonic bodies widespread in the Iberian, Moroccan (109 analyses from north-eastern Morocco,
western High Atlas and from western-central Anti-Atlas), Kabylian and Calabria-Peloritani massifs (14 and 282 analy-
ses, respectively) and with the pre-Hercynian Pan-African plutonites of Algeria (55 analyses). The obtained results show
very strong geochemical affinities only with the Hercynian granitoids of the Iberian Massif (115 analyses from central
Spain and from northern and central Portugal), thus emphasizing a new hypothesis for the provenance of the analysed
pebbles with important paleogeographical consequences. Such a hypothesis of provenance, in fact, shows evidence that
the AlKaPeCa block (i.e. AlboranSpain + KabylidesAlgeria + Calabria + Peloritani massifs southern Italy), at least
during Oligocene times, must have been still in crustal continuity with the Iberian Massif, supposed to be the source area
of the studied plutonic pebbles.
Key words: Morocco, Rif Chain, Oligocene-Miocene deposits, granitoid pebbles, petrography, geochemistry.
Introduction, geological setting and objectives
The provenance of the detrital elements of the Tertiary turbid-
itic successions of the Betic-Maghrebian Chain is commonly
related to the crystalline rocks of pre-Alpine basements, now
included in different tectonic edifices cropping out in the Al-
pine chains along the western Mediterranean (Fig. 1).
Oligocene-Miocene turbiditic flows, in fact, appear to be
linked to the tectonic history of the southern paleomargin of
the European plate, because their provenance is mainly de-
rived from the dismantling of the so-called AlKaPeCa block
(Al = Alboran, southern Spain and northern Morocco, Ka =
Kabylia, Algeria, PeCa = Calabria-Peloritani Arc, sensu
Bouillin et al. 1986) before and during its incipient break-up,
fragmentation and deformation occurred since Oligocene
times (Olivier 1978, 1979; Durand-Delga & Olivier 1988;
Puglisi 1996).
1
This term is here used to represent the internal flysch deposits of the North Africa Flysch Basin (sensu Gelard 1969; Bouillin et al. 1970;
Bouillin 1978) fed by the Internal Domains.
Thus, the detrital modes of sandstone suites characterizing
the Oligocene-Miocene maurétanien flysch
1
of the Betic-Rifi-
an Chain (i.e. Algeciras and Beni Ider Flysch, Spain and Mo-
rocco, respectively), are mainly represented by quartz-felds-
patic compositions and they suggest a provenance from plu-
tonic and/or high rank metamorphic sources (Pendon & Polo
1975; Chiocchini et al. 1978; Guerrera et al. 1989; Rodriguez
1987; Puglisi & Carmisciano 1992; Puglisi et al. 2001;
Zaghloul et al. 2002). In contrast, the coeval terrigenous de-
posits unconformably overlying the MalaguideGhomaride
Units are well characterized by the abundance of quartz grains
and of lithic fragments, with a very low content of feldspars.
So, they appear to be mainly derived from epimetamorphic
sources and from their mainly carbonate Mesozoic-Tertiary
covers (Puglisi et al. 2001; Zaghloul et al. 2003).
Furthermore, in both these types of deposits, in the Betic
Cordillera as well as in the Rifian Chain, it is possible locally
262
GIGLIUTO et al.
to observe several conglomeratic lithofacies containing well
rounded plutonic and high rank metamorphic pebbles. Grani-
toid pebbles, in fact, have firstly been recognized by Olivier et
al. (1979) within the Tertiary cover of the Ghomaride Units
and recently found also within equivalent successions of the
Betic Internal Domain (Martin-Algarra et al. 1995, 2000;
Zaghloul et al. 2003). Successively, similar pebbles have also
been found within conglomerate horizons marking the lower
portion of the maurétanien Beni Ider Flysch (Puglisi et al.
2001; Zaghloul et al. 2002). The presence of similar pebbles
strongly emphasizes a paleogeographical scenario where the
provenance is unequivocally linked to a sedimentary supply
from crystalline sources.
Nevertheless, in the Betic-Rifian Chain, it is difficult to ex-
plain this type of provenance because, up to now, plutonic
rocks have never been recognized within the highest tectonic
units of these tectonic edifices (i.e. the Malaguide and
Ghomaride Units), whereas outcrops of syn- to late-Hercynian
granitic rocks are very common in the Kabylides and in the
Calabria-Peloritani Arc. So, only in the Betic Cordillera and in
the Rif it is problematic to link this type of provenance with
plutonic bodies which are not exposed.
The aim of this paper is to characterize and to detect the
provenance of these plutonic pebbles and the possibility of
their comparison with other similar rocks cropping out in dif-
ferent sectors of the Maghrebian Chain. Thus, the petrograph-
Fig. 1. Tectonic sketch-map of the western Mediterranean area (taken from Balogh et al. 2001). European Units: 1 Spanish and Euro-
pean Foreland (including a Iberian Cordillera), 2 Units of the Spanish-European paleomargin deformed during the Alpine Orogeny
(Pyrenees, Provençal Chain and Alps), 3 Kabylo-Calabride Chain (including the internal units of the Betic Cordillera). African Units:
4 African Foreland (a = gently deformed: Atlas and Trapanese area; b = undeformed: Pelagian Block, Hyblean Plateau and Apulian
Platform), 5 Units of the African paleomargin deformed during the Alpine Orogeny (South-Alpine), 6 African Units deformed dur-
ing Apenninic-Maghrebian Orogeny (Apennines, Sicilian Maghrebian Chain, Rif, Tell and Betic Cordillera). 710 Pennidic, South-
Alpine, Kabylo-Calabride Chain and Apenninic-Maghrebian Chain fronts.
ic and geochemical results obtained for these granitoid peb-
bles, sampled from conglomerate lithofacies of the lower por-
tion of the Beni Ider Flysch and of the Oligocene-Miocene
successions (Fnideq Formation) unconformably overlying the
innermost tectonic units of the Rifian Chain, are compared
with the data available in literature for the syn- to late-Hercyn-
ian plutonic bodies of the Iberian, Moroccan and Kabylian
massifs and also of the Calabria-Peloritani Arc.
Location, sedimentology and petrographic
characters of the conglomerate intervals occurring
within the Beni Ider Flysch and the
Fnideq Formation
The studied plutonic pebbles have been collected from
some conglomerate lithofacies characterizing the lower por-
tion of the Beni Ider Flysch (maurétanien sector of the flysch
basin) and the Ghomaride Complex covers (Fnideq Forma-
tion), both OligoceneMiocene in age.
The following two sample areas have been selected to repre-
sent the conglomerate lithologies of both the above-mentioned
sandstone suites: the Aïn-ech-Choûkâ area (south of the Ksar
es Sghir village, Fig. 2) and the Beni Maâdane area (east of
Tétouan, Fig. 2), where the lower portion of the Beni Ider Fly-
sch and the upper part of the Ghomaride Complex cover are
263
GRANITOID PEBBLES FROM OLIGOCENEMIOCENE DEPOSITS OF THE RIFIAN CHAIN (MOROCCO)
Fig. 2. Geological sketch-map of the northern Rifian Chain (after Zaghloul et al. 2002, modified). Internal Units: 1 Lower Sebtide
Units (Filali and Hacho Units of Ceuta), 2 Upper Sebtide Units (Federico Units), 3 Ghomaride Units with Mesozoic-Cenozoic cov-
er, 4 Dorsale Calcaire. Flysch Domain Units: 5 Predorsalian Units, 6 Massylian Unit (Chouamat-Melloussa Unit) and 78
Maurétanien Units (i.e. Tisirène and Beni Ider Nappes, respectively), 9 Talâa Lakraa Unit, 10 Numidian Flysch. External Rifian
Units: 11 Tangier Unit, 12 Habt and Loukkous Units, 13 alluvial and Pliocene-Quaternary deposits. Symbols: 14 location of
the study sections, 15 hydrographic trace, 16 main strike-slip faults, 17 main overthrust contacts.
mainly represented by conglomerate intervals (Figs. 3 and 4,
respectively).
Sedimentological characters of the conglomerate
horizons with granitoid pebbles
The Aïn-ech-Choûkâ section (about 650 m thick, Fig. 3),
aged Upper OligoceneLower Miocene (Zaghloul et al. 2002),
shows abundant conglomerate lithofacies(disorganized and
organized conglomerates, A
1
and A
2
facies sensu Pickering
et al. 1989, respectively), interbedded with muddy gravels
characterized by scattered pebbles (Zaghloul et al. 2002). This
section has been subdivided (Zaghloul 2002 and by Zaghloul
et al. 2003) into:
l
A first petrofacies, about 150 m thick, formed by clast-
supported and unsorted polygenic conglomerates (plutonic,
volcanic, and metamorphic clasts, with sedimentary pebbles);
l
A second petrofacies, about 190 m thick, represented by
very poorly sorted and well-rounded matrix-supported sedimen-
tary pebbles, cobbles and blocks, with very thick chert-bearing
conglomerate bodies with abundant nummulite-bearing lime-
stone clasts;
l
A third petrofacies, about 300 m thick, made up by cal-
careous conglomerates (cobbles, boulders and blocks of
dolorudites and nodular limestones), locally with white-grey
calcareous olistoliths (5 to 10 m in size) and with boulders of
Verrucano-like red quartzose sandstones. This lithofacies is
almost devoid of crystalline pebbles. At the top of the section,
a pelitic interval (80 m thick) with few arenaceous turbiditic
264
GIGLIUTO et al.
bodies (up to 1 m thick; facies D, E and B
6
of
Pickering et al.
1989, respectively), is present.
In the Beni Maâdane area (Fig. 4) two mainly conglomerat-
ic horizons have been recognized:
1. A lower siliciclastic conglomeratic interval, with crys-
talline pebbles, directly overlying the Paleozoic basement
and/or its Mesozoic carbonate cover and with sedimentologi-
cal characters related to disorganized and organized con-
glomerates facies
of Pickering et al. (1989), indicative of
debris flows and/or highly concentrated turbidity current pro-
cesses;
2. An upper mainly calcareous conglomeratic and aren-
aceous interval, about 150 m thick, made up of matrix and
clast-supported organized and disorganized conglomer-
ates, with thinning- and fining-upward trends and with the
occurrence of plurimetric olistoliths. In this interval medium-
to very coarse-grained sandstone beds (up to 1 m in thickness,
stratified sandstones and gravelly sandstone facies of Pick-
ering et al. 1989) as well as medium- to coarse-grained graded
sandstones with complete or incomplete Bouma sequences
(classical turbidites, sensu Pickering et al. 1989), are
present testifying to transport processes mainly linked to un-
stable high density turbidity currents.
Yellowish-brownish massive clays with thin-bedded and
fine-grained reddish turbidites (about 190 m thick, Fig. 4)
separate the two conglomerate intervals.
Petrographic characters of the plutonic pebbles
The petrographic characters of 7 selected samples of less-
weathered plutonic pebbles were performed by means of
modal analyses (about 1200 points per sample) in order to de-
tect the paragenesis and to classify the rock types (Table 1).
The analysed plutonic pebbles (4 collected from the Beni
Ider Flysch and 3 from the Ghomaride Complex cover, i.e.
Fnideq Formation), ranging in size from 3 to 10 cm, can be
ascribed to the two-mica, cordierite-bearing monzogranite up
to leuco-monzogranite clans. Their occurrence is high in the
lower portions of the Beni Ider Flysch (about 1015 % of the
total clast population at the base of the Aïn-ech-Choûkâ sec-
tion) and of the Ghomaride Complex covers (up to 25 % of
frequency within the lower siliciclastic conglomeratic interval
of the Beni Maâdane area).
These granitoid pebbles show a massive fabric, an in-
equigranular structure, mainly medium- (0.250.5 mm) to
fine-grained and a hypidiomorphic to subhypidiomorphic tex-
ture.
The quartz (~ 33 %), usually as aggregates of anhedral crys-
tals, slightly zoned and commonly subhypidiomorphic plagio-
clases (~ 27 % with An
2025
), K-feldspar (~ 27 %, mainly
perthitic orthoclase and microcline) and small amounts of
muscovite and biotite are the most important mineral phases.
These values, in agreement with the mean of 14 samples of
granitoid pebbles studied by Puglisi et al. 2001 (quartz
~ 41%, plagioclase ~ 38% and K-feldspar ~ 21%), character-
ize a paragenesis not much different between all the studied
granitoid pebbles. In fact the BM
12
, sample, which is clearly
distinquished from the bulk of the other six samples by differ-
Fig. 3. Simplified stratigraphic column of the Oligocene-Miocene
Beni Ider Flysch in the Aïn-ech-Choûkâ section (after Zaghloul et
al. 2002, modified). 1 Turbiditic facies, 2 location of the
analysed pebbles, 3 positive cycles, 4 very poorly sorted and
well-rounded matrix-supported pebbles, 5 unsorted clast-sup-
ported conglomerates.
265
GRANITOID PEBBLES FROM OLIGOCENEMIOCENE DEPOSITS OF THE RIFIAN CHAIN (MOROCCO)
Fig.
4.
Geological
sketch
map
of
the
Beni
Maâdane
area
(Internal
Rif,
Morocco;
after
Zaghloul
et
al.
2003)
showing
the
mainly
conglome
ratic
Oligocene-Miocene
deposits
of
the
Ghomaride
Com-
plex
covers.
1
Pliocene
and
Quaternary
deposits.
Oligocene-Miocene
deposits
of
the
Ghomaride
Complex
cover:
Upper
Conglomeratic
Interval:
2
calcareous
conglomerates,
3
m
ixed
con-
glomeratic
lithofacies
(siliciclastic
and
calcareous),
4
siliciclastic
conglomerates;
Lower
Conglomeratic
Interval:
5
m
arls,
6
siliciclastic
conglomerates,
7
limestones
and
dolostones
(Upper
Triassic
to
Lower
Lias),
8
Verrucano-like
red
clays,
sandstones
and
conglomerates
(Triassic).
9
Paleozoic
basement
of
the
Ghomaride
Units:
(a
) Beni
Hozmar
and
(b
) A
âka
ïli
Nappes,
10
nappe
stacking
contacts,
11
low
angle
normal
faults,
12
high
angle
normal
faults,
13
strike-slip
faults.
Right
side:
simplified
stratigraphic
section
of
the
Beni
Maâdane
outcrop
(Oligocene
A
quitanian;
Internal
Rif,
Morocco).
1a
C
alcareous
conglomerates
and
chaotic
facies,
1b
arenaceous
lithofacies,
1
c
lower
siliciclastic
conglomeratic
interval,
2a
pelitic
lithofacies,
2
b
m
etric
olistoliths,
3
grain
size
in
ϕ
scale,
4
location
of
the
analysed
samples,
56
positive
and
negative
cycles,
respectively.
266
GIGLIUTO et al.
ent geochemical properties, is also microscopically very simi-
lar to the other granitoid pebbles. It shows, in fact, abundant
quartz (~ 41 %), subordinate amounts of K-feldspar (~ 30 %)
and of plagioclase (~ 17 %) and its state of preservation is
good, with very scarce traces of alteration only testified by
few plagioclase crystals very slightly involved in sericitiza-
tion processes. These same very rare traces of alteration are
also locally present within the other samples and, for this rea-
son, we do not believe that they could be responsible for the
geochemical difference of the BM
12
sample, whose distinctive
character will be successively discussed and tentatively ex-
plained.
Furthermore, in all the analysed samples very few heavy
minerals (i.e. zircon, tourmaline, magnetite and rare apatite,
usually never more than 0.81 %) and very small amounts of
other products, probably derived by deuteric alteration mainly
from plagioclases, have been observed to constitute the com-
plementary characteristic mineral assemblage of these rocks.
Myrmekitic textures also occur and, locally, very sporadic
traces of a probably green-schist metamorphic overprint have
been recognized. An association of albite + white mica + epi-
dote + chlorite, that is not pervasive and does not obliterate
the original magmatic texture, is evidence of this.
Geochemical characters of the granitoid pebbles
and their comparison with similar rocks of the
Betic-Maghrebian Chain and of the Iberian Massif
Table 2 lists the analytical data of major-oxides, trace and
rare earth elements (REE), determined in 7 granitoid pebbles
and performed at the Activation Laboratories (Canada)
2
.
Plutonic pebbles of the Oligocene-Miocene deposits of the Rifian Chain
Plutonic bodies of the Calabria-
Peloritani Arc
New data
Ghomaride Complex covers
Beni Ider Flysch
Ghomaride Complex covers
Beni
Maâdane
(n = 12)
1
Gharrabo
(n = 19)
1
Sila
Batholith
(n = 65)
2
Serre
Batholith
(n = 41)
3
Aspromonte
Batholith
(n = 485)
4
VU
4
CR
1
AC
8
AC
22
BM
12
CR
8
CR
10
x
ó
x
ó
x
x
x
Quartz
35.4 32.3 29.7 28.5
41.1
31.9
34.3
31.9 3.0
32.8
2.4
31.2
29.6
33.7
Plagioclase
23.7 31.1 33.6 29.8
17.4
24.1
28.1
22.8 3.2 316
2.2
34.3
40.5
37.2
K-feldspar
28.3 26.2 23.2 27.0
29.9
27.3
24.9
21.0 4.4 214
4.2
21.3
14.6
16.5
Biotite
3.5 4.9 7.5 9.7
1.9
10.4
3.8
7.3 1.7
6.5
1.7
8.1
12.8
6.3
Muscovite
6.6 3.7 4.1 3.1
8.1
4.3
7.7
7.8 3.5
6.6
1.0
4.3
1.6
5.7
Cordierite
- 0.5 0.8 0.7
-
0.5
-
0.8 0.5
0.4
0.3
0.1
-
tr
Opaque minerals
1.7 1.1 0.7 1.2
0.9
1.2
1.2
0.3 0.1
0.3
0.1
0.2
-
-
Accessory minerals
0.8 0.2 0.4 -
0.7
0.3
-
0.2 0.1
0.2
0.1
0.6
0.3
0.7
100.0 100.0 100.0 100.0
100.0
100.0
100.0
x and σσσσσ average and standard deviation, respectively; n number of analysed samples; tr traces. 1 analyses from Martin-Algarra et al.
(2000); 2 mean of two means from 65 analyses (Lorenzoni et al. 1979; Martin-Algarra et al. 2000); 3 mean of four means from 41 modal
analyses (Moresi & Paglionico 1975; Martin-Algarra et al. 2000); 4 mean of four means from 485 modal analyses (Puglisi & Rottura 1973;
Messina et al. 1974; Crisci et al. 1979; Ioppolo & Puglisi 1980. Authors emphasize the presence of sillimanite and of traces of andalusite and
cordierite within the 20→92 % and the 1→15 % of the samples, respectively).
Table 1: Modal point counts of the analysed granitoid pebbles compared with other plutonic rocks of the Calabria-Peloritani Arc.
2
Major-oxides (all with 0.01 % detection limits) and the Sc content
have been determined by ICP, whereas trace elements together with
rare earth elements have been performed by ICP/MS.
Fig. 5. SiO
2
vs. major-oxides and trace elements variation dia-
grams for the analysed plutonic pebbles.
267
GRANITOID PEBBLES FROM OLIGOCENEMIOCENE DEPOSITS OF THE RIFIAN CHAIN (MOROCCO)
Table 2: Major-oxide composition and trace element contents of the analysed granitoid pebbles.
VU
4
CR
1
AC
8
AC
22
B
M
12
CR
8
CR
10
SiO
2
72.72
72.66
74.11
73.44
77.93
72.23
71.49
TiO
2
0.16
0.20
0.13
0.30
0.05
0.26
0.28
Al
2
O
3
14.21
14.29
14.22
13.67
12.06
14.68
14.48
Fe
2
O
3
1.70
1.58
0.69
2.17
0.42
1.93
1.93
MnO
0.02
0.02
0.01
0.03
0.01
0.02
0.02
MgO
0.52
0.41
0.19
0.56
0.13
0.63
0.61
CaO
0.87
0.73
0.56
0.73
0.38
1.09
1.04
Na
2
O
2.79
2.83
3.29
2.98
3.49
3.13
2.99
K
2
O
5.02
5.29
5.69
4.76
4.88
4.58
4.82
P
2
O
5
0.20
0.15
0.23
0.18
0.02
0.17
0.17
LOI
1.77
1.26
0.82
1.15
0.65
1.36
1.26
tot
99.98
99.42
99.94
99.97
100.02
100.08
99.09
Trace elements in p. p. m
.
detection limits
VU
4
CR
1
AC
8
AC
22
B
M
12
CR
8
CR
10
Zr
0.1
103
126
57
106
74
118
115
Hf
0.1
2.9
3.6
2.0
3.0
3.7
3.3
3.3
Ta
0.01
2.7
3.0
3.9
1.9
3.8
1.9
1.9
Nb
0.5
12
15
15
14
14
12
12
La
0.01
19.1
27.9
9.4
22.8
14.0
21.2
22.4
Ce
0.01
37.7
54.9
19.5
47.8
44.9
44.3
49.3
Nd
0.01
15.9
23.3
8.1
21.4
14.4
19.8
21.5
Eu
0.005
0.50
0.58
0.49
0.46
0.13
0.54
0.57
Sn
0.5
17
18
12
9
3
9
8
Tb
0.01
0.4
0.6
0.3
0.7
1.1
0.4
0.5
Yb
0.01
1.0
1.7
0.5
2.0
4.7
1.0
1.0
Lu
0.002
0.14
0.23
0.07
0.27
0.68
0.15
0.15
Y
0.1
12
16
5
20
48
11
11
Th
0.05
9.8
12.8
4.9
11.4
19.0
12.0
12.5
U
0.05
3.1
3.8
1.8
2.3
2.2
2.2
2.2
Ba
0.1
256
296
253
170
122
249
279
Rb
0.1
318
310
300
289
125
257
267
Sr
0.01
128
130
88
52
34
101
102
Ga
1
20
21
16
20
19
19
19
Cs
0.1
36.9
32.3
11.9
30.7
0.9
22.3
21.4
Sc
2 p.p.m.
2
3
2
5
3
4
4
The analysed granitoid pebbles show uniform major-oxide
composition and trace element contents, characterized by a
narrow range of SiO
2
(71.4977.93 wt. %), by high Al
2
O
3
(> 14 %) and A/CNK > 1 (comprised in the range 1.01.3),
by low contents of femic elements [(TiO
2
+ FeO
tot
+ MgO)
< 3 %] and of CaO, Sr, Ba, and by relatively high contents of
K
2
O, Rb, Cs, Ta (Table 2). In addition, they are also charac-
terized by a Th/U ratio ranging from 2 to 9 and by a relatively
low content of ΣREE with an Eu anomaly and scattered
HREE.
In the SiO
2
vs. alkali diagram all the samples exhibit a sub-al-
kaline character (K
2
O/Na
2
O ranges from 1.40 to 1.87), display-
ing a calc-alkaline affinity (high Al
2
O
3
, K
2
O and low TiO
2
).
Compared to the major elements, the ranges of variation ob-
served for the trace elements are much greater. In the SiO
2
vs.
major-oxides and trace elements variation diagrams (Fig. 5) it
is possible to observe the distribution of the data points rather
scattered in every case, but characterized by a continuous
variation of composition within the population for six of anal-
ysed samples. Then, except the BM
12
sample, a single popula-
tion of samples well marked by a negative correlation for
TiO
2
, Al
2
O
3
, Fe
2
O
3tot
, MgO, CaO, REE, Sr, Ba, Th/U, Zr, Hf
and by a positive correlation for Na
2
O, K
2
O and Rb may be
recognized.
Moreover, before listing the geochemical data obtained and
discussing their geological significance, we must underline
that it could be very difficult to use the chemical data of the
analysed pebbles to detect their tectonic setting, because pos-
sible mechanisms of alteration could have affected the rocks
during the sedimentary processes and, probably, also modi-
fied their primary composition.
Nevertheless, we think that the primary composition of the
analysed granitoid pebbles is substantially unchanged because
the observed correlations (Fig. 5) seem to follow the common
granitic trends. Alterations, in fact, are expected to produce a
strong scattering within these trends.
The REE patterns are shown in Fig. 6. They are fractionated
with a moderate Eu anomaly displaying congruent LREE pat-
tern but HREE very scattered. Five samples show a common
pattern typical of S-type granites. The AC
8
sample shows
lowest REE, probably owing to still less occurrence of acces-
sory minerals such as zircon: in fact, it also shows strong de-
pletion of Zr, Y and Th. The BM
12
sample shows strong Eu
anomaly and higher HREE contents.
However, the observed chemical characters are consistent
with the hypothesis of a common origin and provenance for
six of the analysed samples. One of them (BM
12
sample), in-
stead, has clearly distinct composition. In the diagram of Fig. 7
268
GIGLIUTO et al.
(Batchelor & Bowden 1985), in fact, the BM
12
sample falls in
the post-orogenic granite field, while the other samples plot in
the syn-collision granite field.
Furthermore, some chemical characters of this sample (high
SiO
2
, Y, HREE, low Al, Ca, Ba, Sr and largest negative Eu
anomaly) are similar to those of A-type granites, which are
well characterized by high Ga/Al ratio and high
ΣZr + Nb + Ce + Y values (usually > 2.6 and > 350, respec-
tively; Whalen et al. 1987). The BM
12
sample, in particular,
shows a high Ga/Al ratio (about 3.0) but coupled with a
ΣZr + Nb + Ce + Y = 181 and also with a lower Sn content.
Nevertheless, its Ga content is not higher than that of the oth-
er samples, characterized by a Ga/Al ratio in the range 2.1
2.8 and by a ΣZr + Nb + Ce + Y in the range 97212.
Therefore the classification of the BM
12
sample is dubious.
In order to identify the provenance of the studied pebbles,
their analytical data have been compared with those of syn- to
late-Hercynian granitoids coming from the Calabria-Pelori-
tani Arc (282 analyses: Ayuso et al. 1994; Barone 2000; Cag-
gianelli et al. 1994; Crisci et al. 1979; Fornelli et al. 1994;
Ioppolo & Puglisi 1980; Messina et al. 1991a,b; Rottura et al.
Fig. 8. Variation diagrams showing the Sr, Rb and Ba contents of the
analysed pebbles compared with the syn- to late-Hercynian plutonic
rocks of the Calabria-Peloritani Arc and of the Kabylian massifs.
1989b, 1991) and from the Kabylian massifs (14 analyses:
Peucat et al. 1996).
The composition of the studied rocks overlaps the composi-
tional field of the compared samples, with regard to major and
some trace elements, but the Rb, Sr and Ba contents are rather
different. The analysed pebbles (except the outsider one) show
a higher Rb and lower Sr and Ba contents than the granitoids
of the Calabria-Peloritani Arc and of the Kabylian massifs
(Fig. 8). It is highly unlikely to link the contents of these ele-
ments to possible mechanisms of alteration responsible for a
loss of Sr and Ba accompanied by an increase of Rb, as a kind
of K-Rb metasomatism, which can occur only with great diffi-
culty in hypergene conditions. Moreover, the analysed grani-
toid pebbles could contain carbonate products of alteration,
which would produce an increasing of the Sr content rather
than its decrease. That seems to be testified by the good corre-
lation of CaO vs. Loss on Ignition (this last also including
Fig. 9. CaO vs. LOI diagram showing a positive correlation.
Fig. 7. R
1
= [4Si11(Na+K)2(Fe+Ti)] vs. R
2
= (6Ca+2Mg+Al)
diagram showing the geological setting discrimination of different
granitoid rock series. For symbols see Fig. 6.
Fig. 6. Chondrite-normalized variation diagram showing the REE
patterns of the analysed pebbles.
269
GRANITOID PEBBLES FROM OLIGOCENEMIOCENE DEPOSITS OF THE RIFIAN CHAIN (MOROCCO)
some CO
2
, Fig. 9). For this reason it is improbable that the
granitoids of the Calabria-Peloritani Arc and of the Kabylian
massifs represent the source lithotypes of the studied pebbles.
Then, we compared the pebble data with those of Hercynian
and/or pre-Hercynian granitoids coming from the Iberian Mas-
sif (central Spain and northern and central Portugal, 115 anal-
yses: Bea et al. 1994; Holtz & Barbey 1991; Mendes & Dias
1996; Neiva et al. 1987; Ramirez & Menendez 1999; Rottura
et al. 1989a; Wickham 1987) and from the Morocco (north-
eastern Morocco, western High Atlas and western-central
Anti-Atlas; 109 analyses: Ajaji et al. 1998; Barbey et al. 2001;
Eddif et al. 2000; El-Khanchaoui et al. 2001; Gasquet et al.
1992; Mortaji et al. 2000) as well as with the Pan-African plu-
tonites of the Algeria (55 analyses: Cheilletz et al. 1992; Hadj-
Kaddour et al. 1998; Kesraoui & Nedjari 2002).
The granitoids from Morocco show high Sr and Ba con-
tents, higher than the studied pebbles, whereas the granitoids
from Algeria show very scattered Rb contents of > 600 ppm
(until 1698 ppm). The Rb, Sr and Ba contents of the studied
pebbles are only quite equivalent to those of the Iberian Mas-
sif granitoids (Fig. 10) as well as the other geochemical char-
acters (i.e. major-oxide composition and trace elements).
The Hercynian granitoids of Iberia (Spain and Portugal)
have been subdivided, on the basis of their relationships with
the main deformation events, into older syn-tectonic and
younger post-tectonic granitoids (Oen 1958, 1970; Schermer-
Fig. 10. Variation diagrams showing the Sr, Rb and Ba contents of
the analysed pebbles compared with the Hercynian plutonic rocks
of the Iberian and Moroccan massifs and with the pre-Hercynian
plutonites of Algeria.
horn 1959). The studied pebbles exhibit chemical characters
similar to those of syn- and post-collision granitoids.
So, in conclusion, the geochemical data obtained and the re-
sults of this comparison with many Hercynian and pre-
Hercynian plutonic products characterizing the western peri-
Mediterranean chains and their foreland areas allow us to admit
that the analysed pebbles could well be mainly compared with
the Hercynian granitoids of the Iberian Massif.
Conclusions
Petrographic affinities between granitoid pebbles very simi-
lar to those described here and the syn- to late-Hercynian plu-
tonites of the Calabria-Peloritani Arc have been many times
emphasized by studying the conglomeratic horizons of the
Oligocene-Miocene covers of the Ghomaride/Malaguide com-
plexes (Betic-Rifian Chain, Martin-Algarra et al. 1995, 2000;
Zaghloul et al. 2003) and of the coeval more external deposits
(Beni Ider Flysch), first recognized by Puglisi et al. 2001.
Also in this study the results of the modal analyses show a
very close similarity between the composition of these pluton-
ic pebbles (two-mica, cordierite-bearing monzogranite up to
leuco-monzogranite) and that of the above mentioned plutonic
bodies of the Calabria-Peloritani Arc, thus confirming the pre-
vious data collected by Puglisi et al. 2001.
Nevertheless, the comparison of some geochemical charac-
ters (mainly the Rb, Sr and Ba contents) seems to exclude the
possibility of correlating the analysed granitoids with the plu-
tonic rocks of the Calabria-Peloritani Arc and of the Kabylian
massifs and, of course, to consider these areas as possible sed-
iment sources. In the same way, the Hercynian plutonism
characterizing the Moroccan (north-eastern Morocco, western
High Atlas and western-central Anti-Atlas), as well as the
Pan-African plutonites of Algeria, appear to be very different
in geochemical composition from the analysed granitoid peb-
bles and so these rocks cannot be identified as source areas.
In contrast, the comparison with the Hercynian granitoids of
the Iberian Massif (central Spain and northern and central Por-
tugal) shows a very strong geochemical affinity with the plu-
tonic pebbles described in this study.
Thus, owing to the small number of analysed granitoid peb-
bles, it is very difficult to support new hypotheses of prove-
nance even if the above mentioned geochemical affinities
could suggest a new paleogeographical scenario, where these
granitoid pebbles could be closely linked to the Iberian Mas-
sif. These results seem to re-open the debate concerning the
source areas of the granitoid pebbles found in sedimentary
successions belonging to two adjacent paleogeographical do-
mains (Internal Domain and Flysch Basin Domain of the Rif
Chain) and they show two possible provenances.
The first one (Martin-Algarra et al. 1995, 2000) is related to
a sediment source formed by a presently lost continental
crust realm, originally located very near to the Malaguide/
Ghomaride Domain. In this case, the plutonic sources are
completely lacking in outcrop and, up to now, they have not
been found because they are now (1) buried and/or obliterated
under thick Miocene successions or (2) collapsed and sub-
merged in the Alboran Sea. In this way, we suggest that the
270
GIGLIUTO et al.
few but significant geochemical results of this study which
provide evidence of igneous rocks forming this lost conti-
nental crust realm more similar to the Hercynian plutonites
of the Iberian Massif rather than those of the Calabria-Pelori-
tani Arc and/or of the Kabylides, as hypothesized by Martin-
Algarra et al. (1995, 2000) should not be neglected.
The second possible alternative of provenance is to suppose
the Iberian Massif as the source area of the analysed granitoid
pebbles. In this case, we must hypothesize that, during Late
OligoceneAquitanian times, it could have been an intermit-
tent source area, which sporadically fed small satellite basins
located in the more elevated portions of the folded overthrust
belt (i.e. the Ghomaride Units, Zaghloul et al. 2003). That
seems to be testified by the presence of episodic conglomerate
horizons with granitoid pebbles, interbedded within the main-
ly arenaceous-pelitic succession of the Ghomaride Complex
covers. According to the scarcity of feldspar grains within the
sandstones (Zaghloul et al. 2003), in fact, the provenance of
the whole succession has mainly been linked to the same
Ghomaride realm rocks (metasedimentary and epimetamor-
phic rocks with carbonate covers), rather than to plutonic
sources.
Furthermore, it is possible to admit that also the provenance
of the Beni Ider Flysch is closely related to the Iberian Massif,
and probably to its pre-Betic cover, at least for the lower por-
tion of the succession where the composition of the sand-
stones is enriched in feldspars and where the coarse- to very
coarse-grained (up to conglomerate) lithofacies shows an
abundance of plutonic pebbles (Puglisi et al. 2001; Zaghloul
et al. 2002).
In conclusions, if this second hypothesis of provenance is
supported and confirmed by further data, than we could imag-
ine a paleogeographical scenario consisting of a drainage ba-
sin made up also by the Iberian Massif terranes.
Acknowledgments: Financial support was provided by the
Italian MURST as grants to D. Puglisi and to F. Lentini (Cofin
2002, U.R.F. Lentini, University of Catania, Italy), by the
U.F.R. Géologie Méditerranéenne grant to M.N. Zaghloul
(Université AbdelMalek Essaadi Faculté des Sciences Tét-
ouan, Morocco) and by the Geophysics and Georesources
Group grant to A. Ouazani-Touhami (Université Abdel-
Malek Essaadi Faculté des Sciences Tétouan, Morocco).
The authors wish to thank I. Petrík (Geological Institute of
the Slovak Academy of Sciences of the Slovak Republic) and
Ph. Olivier (University of Toulouse, France), whose useful
suggestions strongly improved the manuscript.
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