www.geologicacarpathica.sk
Introduction
The evolution of Cretaceous carbonate platforms was influ-
enced by global changes in the carbon cycle, climate and ma-
rine productivity (Schlanger & Jenkyns 1976; Weissert et al.
1998; Steuber 2002; Steuber & Veizer 2002).
Trace elements and carbon isotope stratigraphy realized in
pelagic and hemipelagic carbonate successions combined with
sedimentological analysis have been conducted to recognize
systems tracts and sea-level changes for Cretaceous time (Jen-
kyns 1995; Bellanca et al. 1996; Perez-Infante et al. 1996;
Weissert et al. 1998; Kump & Arthur 1999; Masse et al. 1999;
Jarvis et al. 2001).
However, chemostratigraphy of shallow-water carbonate
sediments remains understudied because the sedimentary
record is often discontinuous and the geochemical data repre-
sents a combination of several signals, such as the deposition-
al paleoenvironments, the paleosalinity and the influences of
diagenesis, particularly important in these sediments (Vincent
et al. 1997, 2004). The water-rock interaction of the diagenetic
processes can modify the significance of the original chemical
Meteoric diagenesis of Upper Cretaceous and Paleocene—
Eocene shallow-water carbonates in the Kruja Platform
(Albania): geochemical evidence
GRIGOR HEBA
1
,
GILBERT PRICHONNET
1
and ABDERRAZAK EL ALBANI
2
1
Département des Sciences de la Terre et de l’Atmosph
č
re et GEOTERAP, Université du Québec
ŕ
Montréal, C.P. 8888 succursale centre-
ville, Montréal, Québec, H3C 3P8, Canada; grigorheba@hotmail.com
2
UMR 6532-Hydrasa, Université de Poitiers, UFR SFA, Bât. Sciences Naturelles, 40, avenue du Recteur Pineau, F-86022 Poitiers Cedex, France
(Manuscript received March 25, 2008; accepted in revised form October 23, 2008)
Abstract: In the central part of the Kruja Platform (Albania) located in the Apulian passive margin, geochemical
analyses (calcimetry, Sr, REE and isotopic,
δ
13
C and
δ
18
O) coupled with sedimentological and sequence stratigraphic
study were carried out on Upper Cretaceous (CsB4, CsB5, CsB6 Biozones) and Paleocene to Middle Eocene shallow-
water carbonates that crop out in the Kruje-Dajt massif (L’Escalier section) and Makareshi massif (La Route section).
The lower values in Sr contents, the homogeneous
δ
18
O values in both sections and the covariance between
δ
13
C and
δ
18
O values (La Route section) are attributed to diagenesis influence by a meteoric water-buffer system, supported by
petrographic observations. Moreover, a new exposure surface during the Late Cretaceous time (between CsB5 and
CsB6 Biozones) may be proposed according to the low or negative excursions of Sr values, the negative excursions of
isotopic values in both sections and a positive peak of normalized REE values (La Route section). These variations
correlate with the geochemical signal reported by the decreasing strontium isotope values of rudist shells in the Island
of Brač carbonate platform (Apulia domain) during the late Middle Campanian (77.3 Ma). Also, this continental expo-
sure is consistent with the global
sea-level fall reported from the Boreal Realm, North Atlantic, and the southern Tethyan
margin. This geochemical evidence is a complementary tool for the sedimentological analysis and suggests a maximum
regression (a sea-level fall) at the transition between the CsB5 and CsB6 Biozones. The high values of Sr content in
Middle Eocene carbonates (L’Escalier section) reflect changes in depositional environment from restricted to open
marine conditions. REE values increase through transgressive systems tract, characterized by small increase of detrital
input. However, anomalies of certain values in both sections suggest disturbances linked either to the changes in clay
input and to diagenetic modifications. Peaks in dolomite content are linked with regressive episodes or tendencies, and
dolomitic facies, as indicated by intertidal-supratidal depositional environments.
Key words: Late Cretaceous, Paleocene, Middle Eocene, Albania, Kruja Platform, diagenesis, geochemistry,
sedimentology, shallow-water carbonates.
signal by the recrystallization of carbonate minerals. The oxy-
gen isotope record in the Mesozoic and older carbonate rocks
needs to be interpreted with cautions, because it is the product
of the original record and an unknown input by meteoric water
influx later, during post-depositional diagenetic alteration at
elevated temperature, between 40° and 50° according to Sheu
(1990) and Marshall (1992). Moreover, the carbon isotopic
signal in Cretaceous carbonate platform is poor, often show-
ing high-amplitude fluctuations because of the diagenetic
overprint which complicates the identification of the time and
nature of the events causing those variations (Joachimski
1994; Buonocunto et al. 2002). To overcome these problems,
a multidisciplinary approach involving stratigraphic, sedimen-
tological and geochemical data is recommended by several
authors (Joachimski 1994; Vincent et al. 1997, 2004; Buono-
cunto et al. 2002).
This study presents geochemical data for the Upper Creta-
ceous and Paleocene to Middle Eocene carbonates of the
Kruja Platform, a folded and overthrust zone which is recog-
nized from South to North in Albania (Papa 1972; I.S.P.GJ.
& I.GJ.N. 1983; Meço & Aliaj 2000; Robertson & Shallo
GEOLOGICA CARPATHICA, APRIL 2009, 60, 2, 165—179 doi: 10.2478/v10096-009-0011-6
è
à
166
HEBA, PRICHONNET and EL ALBANI
Fig. 1.
Location, lithology and sequence stratigraphy of the studied s
ections (L’Escalier and La Route), and biostratigraphy of the L
ate Cretaceous to Eocene interval of the Kruja Platform (Al-
bania).
After
I.S.P.GJ.
&
I.GJ.N.
1983;
and
Heba
&
Prichonnet
(2006).
Legend:
Fig. 2.
167
METEORIC DIAGENESIS OF CRETACEOUS—EOCENE SHALLOW-WATER CARBONATES (ALBANIA)
2000): this platform is located in the Apulian passive margin
which extended on both sides of the Adriatic and Ionian Sea
(Fig. 1).
The two main objectives are: (1) to compare these results
with the sedimentological and sequential results of this time
interval where two periods of emersion are recognized, as de-
scribed in Heba & Prichonnet (2006); and (2) to determine the
relationship between the geochemical signal, depositional en-
vironments and diagenesis.
To achieve these goals, two sections of this platform have
been analysed for carbonates, strontium and stable isotope
(
δ
13
C and
δ
18
O) content, and Rare Earth Elements (REE). The
two sections presented there are the same as in the Heba &
Prichonnet (2006): (a) the L’Escalier section in the Kruje-Dajt
massif is composed of 360 m of limestones and 240 m of do-
lomitic rock; and (b) La Route section in the Makareshi massif
includes 126 m of limestones and 49 m of dolomitic rock.
Sample spacing was relatively large, representing only major
facies and environmental changes, previously defined using
sedimentological criteria, which should be coupled with
geochemical signatures.
Geological setting
The studied sections cover the Late Santonian to the Early
Maastrichtian stages of the Late Cretaceous, from 86 Ma to
70 Ma. Then both sections display a gap, the L’Escalier sec-
tion extends into the Paleogene up to the Middle Eocene and
the La Route section only to the Middle Eocene. Finally, Up-
per Eocene marls (in several locations) and Oligocene flysch
cover the platform carbonates (starting at 39.4 Ma).
For the whole carbonate sequence, the biostratigraphic
framework is mainly based on benthic foraminifers. The Late
Cretaceous is divided into four biozones (Heba 1997; Heba &
Prichonnet 2006) based on species of the Rhapydioninidae
family (Fleury 1980), namely CsB4 (Late Santonian-Campa-
nian), CsB5 (Early Campanian), CsB6 (Late Campanian—Ear-
ly Maastrichtian) and CsB7 (Late Maastrichtian). With regard
to the Tertiary, it is characterized by typical Paleocene and
Middle Eocene miliolids and large hyaline foraminifers (Gjata
et al. 1968; Peza 1973, 1977, 1982).
The stratigraphic succession is dominated by Upper Creta-
ceous neritic carbonates, limestones and dolomites, containing
benthic foraminifers that were deposited in a confined subtidal
to supratidal environment (Papa 1972; Peza 1973, 1975, 1977,
1982; I.S.P.GJ. & I.GJ.N. 1983; Heba 1997; Meço & Aliaj
2000; Robertson & Shallo 2000; Heba & Prichonnet 2006).
Local variations of environments between the two sections are
attributed to minor and common fluctuations of carbonate
platforms, mainly due to facies succession; and in two periods
of time, to eustatic variations which had caused two emer-
gences (regressions) and temporal discontinuities at the end of
the Cretaceous and Early Eocene times, also with some differ-
ences between the two sections. The major regression in the
Kruja Platform began at the end of the Early Maastrichtian
and extended for about 3 Myr in the L’Escalier section, where
the CsB7 foraminiferal Biozone (Late Maastrichtian) is miss-
ing (Heba 1997; Heba & Prichonnet 2006), and about 20.5 Ma
in the La Route section creating a gap ranging from Biozone
CsB7 to the Early Eocene. Evidently these gaps include large-
ly the Cretaceous/Tertiary boundary. The second regression is
characterized by the presence of bauxite, but is only observed
in the L’Escalier section: it lasted about 5 Myr during the Ear-
Fig. 2. Sedimentary depositional model of the facies succession (after Heba & Prichonnet 2006) and legend key.
168
HEBA, PRICHONNET and EL ALBANI
ly Eocene. At the top of carbonate sequence in both sections,
the Middle Eocene consists of organogenic limestones, depos-
ited in an open shallow subtidal environment.
Sedimentological and sequence stratigraphical
analysis
A general introduction to the facies analysis and sedimenta-
ry cycles of the L’Escalier and La Route sections is given
here; further details may be found in Heba & Prichonnet
(2006). The Upper Cretaceous to Paleogene carbonate depos-
changes of facies, maximum flooding surfaces, transgression
surfaces, clearly defined erosional truncation and direct evi-
dence of subaerial exposure. From the recognition of progra-
dational or retrogradational parasequence sets, fourteen
genetic sequences (or cycles) sensu Cross (1988) can be deter-
mined in the L’Escalier section and seven in the La Route sec-
tion (Fig. 1).
The maximum regression happened simultaneously in the
two sections, at the thirteenth genetic sequence level (S13) in
the L’Escalier section and at the sixth genetic sequence level
(S6) in the La Route section (Fig. 1), characterized by an ex-
posure surface at the end of CsB6 Biozone (Late Campanian—
Table 1: Calcimetry data for L’Escalier and La Route bulk sediment samples.
Sample
CaCO
3
%
(CaMg)CO
3
%
Facies Sample
CaCO
3
%
(CaMg)CO
3
%
Facies
L’Escalier section (Kruje-Dajt massif)
V2 23.88
78.56
F9
V198 24.95
72.93
F8
V3 20.87
81.94
F5
V203 26.22
71.64
F8
V12 15.88 86.95
F1
V208 98.62 F10
V31 21.19 81.62
F4
V208/1 93.13 F10
V32 28.73 72.58
F5
V209 97.18 F10
V36 97.64 F4
V209/1 91.28 F10
V45 89.96 F4
V204 98.77 F11
V54 83.56 F3
V205 83.22 F11
V48 92.50 F4
V206 94.61 F11
V51 81.21 F4
V207 79.58 F11
V57 97.15 F4
V58 91.18 F4 La Route section (Makareshi massif)
V62 87.13 F4
V64 92.07 F4
M10 95.94 F1
V70 88.00 F4
M14 96.21 F1
V74 96.38 F5
M17 99.03 F1
V75 94.51 F5
M20 96.16 F1
V76 92.18 F4
M25 99.31 F1
V83 96.97 F4
M35 95.99 F1
V88 98.40 F4
M41 84.77 F1
V91 99.47 F2
M46 99.37 F1
V96 91.22 F4
M47 98.18 F2
V101 84.22 12.56 F6 M73
95.99
F2
V102 88.25
F6 M92
87.16
F2
V108 88.06
F3 M99
97.22
F1
V110 98.35
F6 M105 98.27
F2
V111 97.61
F6 M109 98.63
F1
V114 96.93
F4 M127 92.31
F2
V120 87.71 3.02 F2 M129 99.33
F4
V124 97.75
F6 M136 88.16
F4
V125 96.48
F6 M142 99.38
F3
V134 94.94
F6 M145 88.50
F4
V136
97.61 F6
Ms16 43.71 55.41
F5
V143 96.52
F4 M186 67.67 32.25 F7
V144 92.75
F6 M186/1 99.85
F4
V146 97.32
F6 M159 92.95
F4
V149 93.19
F4 M171 86.54 9.62 F3
V163 97.22
F4 M172 99.68
F4
V173
15.52
86.91
F7
M174
90.32
1.52
F4
Vs15
29.10
71.99
F8
M177
84.85
9.84
F4
V178
95.23
F4
M179
86.83
7.83
F3
V184 59.20
F4 M191 33.48 65.50 F5
V185
94.04
F4
M194
92.73
6.73
F4
V187 95.76
F4 M201 26.03 73.29 F5
V189 96.80
F4 M205 18.03 61.13 F7
V190 92.64
F4 M209 48.57 50.85 F8
V193 95.59
F4 M210 24.53 68.06 F8
V194
94.10
F4
M211
88.76
4.44
F11
V195 95.74
F4 M211/1 98.63
F11
V197 41.76 57.86 F7
its of L’Escalier and La Route sections
display eleven sedimentary facies (F1 to
F11; Fig. 2), ranging from subtidal to su-
pratidal environments. These facies are
arranged in a related sedimentary model
as suggested by environmental interpre-
tation of the depositional textures
(Fig. 2). The deepest environments are
characterized by limestones showing ob-
lique stratifications (facies 6). Shallow
subtidal environments are represented
by: (1) rudist debris-bearing limestones
(facies 4) which dominate both sections,
(2) rudist patch reef limestones (fa-
cies 3), (3) dolomicrosparites displaying
bioturbation traces (facies 5), and (4)
bioclastic limestones (facies 11) contain-
ing large hyaline foraminifers (Nummu-
lites and Discocyclines). Intertidal
environments are represented by (1) lam-
inated limestones attributed to microbial
mats (facies 1), (2) rudist storm deposit
limestones (facies 2), (3) bird’s-eyes-
bearing dolomites (facies 7), (4) miliol-
ids-bearing limestones (facies 10), and
(5) brecciated dolomites (facies 9) typi-
cal of intertidal channels. Supratidal en-
vironments are represented by laminated
dolomites displaying desiccation cracks
(facies 8). The dolomitic facies (facies 5,
7, 8 and 9) are interbedded with lime-
stone facies in the Late Cretaceous part
of the sedimentary succession and
present idiotopic textures (euhedral, eor-
phyrotopic and eubhedral). These fea-
tures demonstrate dolomitization during
early diagenesis in a sebkha-type su-
pratidal environment (Purser 1980;
Walker & James 2000; Heba & Prichon-
net 2006).
According to the depositional model
of facies succession seven distinctive
parasequences have been identified
(Heba & Prichonnet 2006). Potential
parasequence boundaries can be identi-
fied at this step based on one or more of
the following stratigraphic criteria: sharp
Notes: (a) Facies are indicated; (b) Stratigraphic positions of samples are indicated in Figs. 3 and 4.
169
METEORIC DIAGENESIS OF CRETACEOUS—EOCENE SHALLOW-WATER CARBONATES (ALBANIA)
Early Maastrichtian) (Heba & Prichonnet 2006). Similar epi-
sodes of regression associated with continental diagenesis or
sedimentation (karstic fillings) are reported from the Maas-
trichtian time in other platforms of the Apulia domain (Gavro-
vo-Tripolitza in Greece – Mavrikas 1993 and Landrein et al.
2001; Island of Brač in Croatia – Gušić & Jelaska 1990). So,
this regression recorded in these two sections of the Kruja
Platform can be attributed with confidence to a global eustatic
variation (relative sea-level fall) at the end of the Early Maas-
trichtian time.
Geochemical approach
Methods
A total of 96 bulk sediment samples (Table 1), 60 for the
L’Escalier section and 36 for the La Route section, were se-
lected for geochemical analysis. These provide a relatively
good stratigraphic coverage of each main facies through the
Late Cretaceous to Middle Eocene studied interval.
Calcimeter analysis of carbonates (limestone and dolomitic
facies) was done on all the micrite samples in each section.
The measurements were made with a Bernard-type apparatus
at the Département des Sciences de la Terre et de l’atmosph
č
re
de l’Université du Québec
ŕ
Montréal (UQAM).
Sr, stable isotopes and REE analyses were performed on
samples containing 80 to 100 % calcite (33 samples for the
L’Escalier section and 18 for the La Route section; Table 2).
During sampling, as much as possible, the dolomitic facies
were discarded. Moreover, visible fossils or shell fragments
(Nummulites, Discocyclines and rudists) have not been includ-
ed. Samples were crushed, and powered (5 g of powder) in an
agate mortar to avoid contamination.
Carbon and oxygen isotopic measurements were done at the
Stable Isotope Lab from GEOTOP-UQAM-McGill (Montréal,
Québec) with a Micromass Isoprime
TM
spectrometer with
Multicarb
TM
system. The isotopic results are reported against
the VPDB (Vienna PeeDee Belemnite) international standard.
Average precisions based on replicate analysis of selected
samples or laboratory standards were ± 0.1 ‰ for
δ
13
C and
± 0.2 ‰ for
δ
18
O.
Strontium (Table 2) and REE analyses (Table 3) were done
at the OGS GeoLabs in Sudbury (Ontario) with an ICP-MS
(IM-100) unit for samples prepared by the Open Beaker Di-
gest method (code: OT4, brochure of OGS GeoLabs, 2003).
Lower limits of detection for these trace elements are: 1 ppm
for Sr, 0.05 ppm for La; 0.1 ppm for Ce; 0.04 ppm for Nd;
0.02 ppm for Sm; 0.01 ppm for Gd; 0.01 ppm for Dy; and
0.008 ppm for Er. Samples were digested in an open beaker
using a combination of hydrofluoric, hydrochloric, nitric and/
or perchloric acids. REE abundances were normalized (Ta-
ble 4) to the average of North American Shale Composite val-
ues (NASC) given by Gromet et al. (1984): La = 31.1 ppm;
Ce = 67.03 ppm; Nd = 30.4 ppm; Sm = 5.98 ppm; Gd=5.5 ppm;
Dy = 5.54 ppm; and Er = 3.27 ppm.
Sample Sr
(ppm)
δ
13
C
(
0
/
00
VPDB)
δ
18
C
(
0
/
00
VPDB)
Facies Sample Sr
(ppm)
δ
13
C
(
0
/
00
VPDB)
δ
18
C
(
0
/
00
VPDB)
Facies
L’Escalier section (Kruje-Dajt massif)
V36
303.92
1.67
–2.57
F4
V194
220.19
–0.98
–4.66
F4
V45
319.8
2.72
–2.16
F4
V195
530.7
2.68
–4.48
F4
V54
181.14
–1.63
–2.54
F3
V208
247.84
1.16
–2.42
F10
V48
328.74
2.12
–2.02
F4
V209
253.85
1.45
–2.43
F10
V51
284.61
1.65
–1.77
F4
V204
765.25
1.05
–5.78
F11
V64
262.81
3.12
–2.48
F4
V207
1016.68
1.01
–5.84
F11
V74
292.56
3.39
–3.42
F4
V76
216.04
2.73
–2.79
F4
La Route section (Makareshi massif)
V83
248.31
3.14
–2.44
F4
V88
287.46
2.73
–4.05
F4
M10
351.32
0.90
–2.01
F1
V91
323.64
1.94
–3.95
F2
M46
305.71
–0.38
–2.43
F1
V96
346.63
2.50
–3.19
F4
M47
247.57
–4.05
–3.70
F2
V102
336.22
2.22
–3.94
F6
M92
199.19
–4.06
–3.70
F2
V108
285.78
2.91
–2.86
F3
M99
200.67
–4.13
–3.13
F1
V110
284.99
2.99
–3.43
F6
M105
345.59
–1.49
–3.09
F2
V114
414.6
2.09
–5.27
F4
M109
118.31
–4.30
–3.95
F1
V120
343.15
2.10
–4.17
F2
M127
361.81
–1.41
–3.47
F2
V125
271.15
1.83
–3.48
F6
M129
257.21
–0.51
–3.06
F4
V136
255.91
1.19
–3.69
F6
M136
258.76
1.72
–1.88
F4
V143
288.76
0.46
–4.67
F4
M145
234.51
0.66
–2.13
F4
V146
276.88
1.87
–2.33
F6
M159
281.09
0.66
–2.53
F4
V149
228.13
1.29
–3.39
F4
M171
312.73
1.46
–2.19
F3
V163
301.56
–2.08
–4.10
F4
M177
352.68
1.73
–2.44
F4
V178
188.3
–0.44
–4.93
F4
M179
257.66
1.10
–2.59
F3
V185
516.91
2.57
–2.64
F4
M194
389.64
1.96
–2.55
F4
V190
505.24
1.72
–4.10
F4
M211
318.09
–0.66
–3.80
F11
V193
461.88
1.44
–5.48
F4
M211/1
300.25
–0.56
–3.71
F11
Notes: (a) Facies are indicated; (b) Stratigraphic positions of samples are indicated in Figs. 3 and 4.
Table 2: Carbon and oxygen isotope, and strontium data for L’Escalier and La Route bulk sediment samples.
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à
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HEBA, PRICHONNET and EL ALBANI
Description of geochemical variations
Calcimeter measurements
Calcite is the dominant carbonate mineral in the analysed
micrites of both sections (Table 1, Figs. 3 and 4).
In the L’Escalier section (Table 1), where 60 % of the car-
bonates are limestones, the calcite content is generally be-
tween 75 % and 95 % (for 80 % of analysis). However,
peaks of dolomite ranging from 71.6 to 87 % are identified
in this series of limestones in some samples (Fig. 3): V2, V3,
V12, V31, V32 and V203.
In the La Route section (Table 1), with 75 % limestones,
calcite represents between 85 % and 95 % of the carbonate
content (for 80 % of analyses). Dolomite peaks ranging from
55.4 to 73.3 % are restricted to the CsB6 Biozone, and to the
samples Ms16, M191, M201 and M210 (Fig. 4).
Strontium measurements
Three main features of the Sr contents are observed in the
L’Escalier section (Fig. 5): (1) the fluctuation of lower val-
ues, ranging from 200 to 400 ppm (samples V36 to V178,
Table 2), in Cretaceous limestones corresponding to the
Table 3: Rare Earth Elements (REE) data for L’Escalier and La Route bulk sediment samples.
Sample
La (ppm)
Ce (ppm)
Nd (ppm)
Sm (ppm)
Gd (ppm)
Dy (ppm)
Er (ppm)
Facies
L’Escalier section (Kruje-Dajt massif)
V36 0.22 0.16 0.08 0.02 0.01
F4
V45 0.34 0.65 0.31 0.07 0.09 0.09
0.06
F4
V54 0.27 0.21 0.17 0.03 0.02 0.02
0.01
F3
V48 0.12 0.15 0.06 0.01
F4
V51 0.15 0.20 0.13 0.03 0.01 0.02
0.01
F4
V64 0.49 0.22 0.18 0.04 0.04 0.04
0.02
F4
V74 0.45 0.11 0.12 0.03 0.02 0.02
0.02
F4
V76 0.19 0.11 0.09 0.02 0.02
0.01
F4
V83
0.26 0.09
0.02
0.01
0.01
0.01
F4
V88
0.39 0.08
0.02
0.02
0.01
F4
V91 0.34 0.15 0.22 0.06 0.04 0.04
0.03
F2
V96 0.31 0.15 0.15 0.02 0.03 0.02
0.01
F4
V102
0.2
0.07
0.02
F6
V108
0.27 0.37 0.18 0.04 0.02 0.03
0.02
F3
V110
0.44 0.10 0.06 0.02
F6
V114 0.24
0.06 0.02
F4
V120 0.09
0.07 0.02 0.01
F2
V125
0.2
0.21
0.11
0.02
0.03
0.02
0.02
F6
V136
0.27 0.19 0.14 0.03 0.03 0.03
0.02
F6
V143
0.12 0.11 0.10 0.02 0.01 0.00
F4
V146
0.55 1.10 0.60 0.12 0.10 0.09
0.05
F6
V149
0.2
0.18
0.14
0.04
0.03
0.03
0.02
F4
V163
0.18 0.19 0.10 0.03 0.02 0.01
0.01
F4
V178 0.25
0.06 0.00 0.00
F4
V185 0.22
0.09 0.02 0.00
F4
V190
0.14 0.26 0.14 0.04 0.02 0.02
0.01
F4
V193
0.18 0.08
F4
V194
0.58 0.85 0.54 0.11 0.12 0.12
0.07
F4
V195
0.41 0.24 0.18 0.04 0.02 0.02
0.01
F4
V208
0.38 0.12
0.03
0.02
0.02
0.02
F10
V209
0.28 0.11
0.03
0.02
0.02
0.02
F10
V204
1.28
1.28
0.93
0.2
0.24
0.23
0.15
F11
V207
1.64 1.81 1.25 0.26 0.31 0.29
0.19
F11
La Route section (Makareshi massif)
M10 0.16 0.18 0.10 0.02 0.02 0.02
0.01
F1
M46 0.35 0.28 0.22 0.05 0.06 0.05
0.04
F1
M47 0.28 0.34 0.17 0.03 0.04 0.03
0.02
F2
M92 0.39 0.14 0.11 0.03 0.02 0.02
0.01
F2
M99 0.19 0.36 0.17 0.03 0.04 0.04
0.03
F1
M105
0.41 0.19 0.10 0.02 0.02 0.02
0.01
F2
M109
0.58 1.02 0.54 0.11 0.14 0.12
0.07
F1
M127
0.38
0.78
0.41
0.1
0.1
0.08
0.04
F2
M129
0.49
0.80
0.51
0.1
0.1
0.07
0.03
F4
M136 0.06
0.06
F4
M145
0.35
F4
M159 0.18
0.08 0.01
F4
M171
0.27 0.24 0.17 0.04 0.04 0.03
0.02
F3
M177
0.25 0.14 0.08
0.02 0.02
0.02
F4
M179
0.06 0.05
F3
M194
0.37 0.38 0.22 0.04 0.04 0.04
0.02
F4
M211
0.73
0.63
0.44
0.1
0.12
0.11
0.08
F11
M211/1
0.72
0.60
0.45
0.08
0.1
0.1
0.07
F11
Notes: (a) Facies are indicated; (b) Stratigraphic positions of samples are indicated in Figs. 3 and 4.
171
METEORIC DIAGENESIS OF CRETACEOUS—EOCENE SHALLOW-WATER CARBONATES (ALBANIA)
Fig. 3. Calcimetry profile for the L’Escalier section (Kruje-Dajt massif). Data are listed in Table 1. Legend: Fig. 2. Note: Stratigraphic po-
sition of grouped samples: I – (V32, V36, V45, V54, V48, V51,V57, V58, V62, V64, V70, V74 to V76, V83); II – (V88, V91, V96,
V101, V102,V108, V110, V111, V114, V120, V124, V125); III – (V134, V136, V143, V144, V146, V149, V163); IV – (V173, Vs15,
V178, V184, V185, V187, V189, V190, V193 to V195); V – (V197, V198, V203, V208, V208/1, V209, V209/1, V204 to V207).
CsB4 and CsB5 Biozones; (2) the increase of the Sr con-
tents to about 500 ppm in Biozone CsB6, although there
are some lower values of about 250 ppm in two samples of
facies 10 (V208 and V209; Paleocene miliolids lime-
stones); and (3), the highest values found in nummulites
and discocyclines Middle Eocene limestones (780 ppm in
sample V204 and 1016 ppm in sample V207; facies 11).
In the La Route section (Fig. 6), the Sr curve displays: (1)
mostly values ranging again from 200 to 400 ppm; and (2) a
low value recorded near the top of the CsB5 Biozone
(118 ppm, sample M109). However, in this section stron-
tium values for the Middle Eocene limestones (facies 11) are
much lower than those obtained for the same facies in the
L’Escalier section (e.g. 318 and 300 ppm respectively in
samples M211 and M211/1).
Stable isotope data
In the L’Escalier section (Fig. 5), carbon isotope values
vary from —2.08 ‰ to + 3.39 ‰. Most of the Upper Creta-
ceous limestones display positive
δ
13
C values, but three neg-
ative peaks were recorded in the upper part of Biozone CsB5
(samples V163, V178) and in Biozone CsB6 (sample V194).
Thus, over most of Biozones CsB4 and CsB5,
δ
13
C values
remain around 2 ‰. After a long-term decrease until the top
of the CsB6 Biozone (sample V178), a rapid change back to
positive values is observed (+ 2.57 ‰ in sample V185). Fi-
nally, after a
δ
13
C negative excursion (—0.98 ‰ in sample
V194) there is a new positive shift (+ 2.5 ‰ in sample
V195). The Tertiary limestones are characterized by
δ
13
C
values near + 1.1 ‰.
172
HEBA, PRICHONNET and EL ALBANI
Table 4: Normalized REE data for L’Escalier and La Route bulk sediment samples.
Sample La
Ce
Nd
Sm
Gd
Dy
Er Facies
L’Escalier section (Kruje-Dajt massif)
V36 0.007 0.002 0.003 0.003 0.002
F4
V45 0.011 0.010 0.010 0.012 0.016 0.016 0.018 F4
V54 0.009 0.003 0.006 0.005 0.004 0.004 0.003 F3
V48
0.004
0.002
0.002 0.002
F4
V51 0.005 0.003 0.004 0.005 0.002 0.004 0.003 F4
V64 0.016 0.003 0.006 0.007 0.007 0.007 0.006 F4
V74 0.014 0.002 0.004 0.005 0.004 0.004 0.006 F4
V76 0.006 0.002 0.003
0.004 0.004 0.003 F4
V83 0.008
0.003 0.003 0.002 0.002 0.003 F4
V88 0.013
0.003 0.003 0.004
0.003 F4
V91 0.011 0.002 0.007 0.010 0.007 0.007 0.009 F2
V96 0.010 0.002 0.005 0.003 0.005 0.004 0.003 F4
V102
0.006 0.002
0.003
F6
V108 0.009 0.006 0.006 0.007 0.004 0.005 0.006 F3
V110 0.014 0.001 0.002 0.003
F6
V114 0.008
0.002 0.003
F4
V120 0.003
0.002 0.003 0.002
F2
V125 0.006 0.003 0.004 0.003 0.005 0.004 0.006 F6
V136 0.009 0.003 0.005 0.005 0.005 0.005 0.006 F6
V143 0.004 0.002 0.003 0.003 0.002
F4
V146 0.018 0.016 0.020 0.020 0.018 0.016 0.015 F6
V149 0.006 0.003 0.005 0.007 0.005 0.005 0.006 F4
V163 0.006 0.003 0.003 0.005 0.004 0.002 0.003 F4
V178 0.008
0.002
F4
V185 0.007
0.003 0.003
F4
V190 0.005 0.004 0.005 0.007 0.004 0.004 0.003 F4
V193
0.006 0.003
F4
V194 0.019 0.013 0.018 0.018 0.022 0.022 0.021 F4
V195 0.013 0.004 0.006 0.007 0.004 0.004 0.003 F4
V208 0.012
0.004 0.005 0.004 0.004 0.006 F10
V209 0.009
0.004 0.005 0.004 0.004 0.006 F10
V204 0.041 0.019 0.031 0.033 0.044 0.042 0.046 F11
V207 0.053 0.027 0.041 0.043 0.056 0.052 0.058 F11
La Route section (Makareshi massif)
M10 0.005 0.003 0.003 0.003 0.004 0.004 0.003 F1
M46 0.011 0.004 0.007 0.008 0.011 0.009 0.012 F1
M47 0.009 0.005 0.006 0.005 0.007 0.005 0.006 F2
M92 0.013 0.002 0.004 0.005 0.004 0.004 0.003 F2
M99 0.006 0.005 0.006 0.005 0.007 0.007 0.009 F1
M105 0.013 0.003 0.003 0.003 0.004 0.004 0.003 F2
M109 0.019 0.015 0.018 0.018 0.025 0.022 0.021 F1
M127 0.012 0.012 0.013 0.017 0.018 0.014 0.012 F2
M129 0.016 0.012 0.017 0.017 0.018 0.013 0.009 F4
M136 0.002
0.002
F4
M145 0.011
F4
M159
0.006 0.003 0.002
F4
M171 0.009 0.004 0.006 0.007 0.007 0.005 0.006 F3
M177 0.008 0.002 0.003
0.004 0.004 0.006 F4
M179
0.002 0.002
F3
M194 0.012 0.006 0.007 0.007 0.007 0.007 0.006 F4
M211 0.023 0.009 0.014 0.017 0.022 0.020 0.024 F11
M211/1
0.023 0.009 0.015 0.013 0.018 0.018 0.021 F11
Notes: (a) Facies are indicated; (b) Stratigraphic positions of samples are indicated in Figs. 3 and 4.
The
δ
18
O curve of the L’Escalier section (Fig. 5) displays
values ranging from —5.84 to —1.77 ‰. In particular, a general
decrease is observed from the base of the section to the end of
the CsB5 Biozone (at the level of V178 sample), followed by
a sharp positive shift. The Tertiary oxygen isotope curve
shows a negative excursion with the lowest value (—5.84 ‰ in
sample V207) at the top of the section. Some samples (V114,
V193, V204 and V207) have
δ
18
O values smaller than —5 ‰,
the limit for marine carbonate deposits in modern sediments
according to James & Choquette (1990).
In the La Route section (Fig. 6),
δ
13
C values range from
—4.30 ‰ to + 1.96 ‰. At the base of the section, most
δ
13
C
values are negative with a peak of —4 ‰ (sample M109) near
the top of Biozone CsB5. A positive excursion follows, shift-
ing to values of circa + 1 ‰ (samples M127, M129 and
M136). Above this positive excursion,
δ
13
C values mainly
fluctuate between 0.6 ‰ and 1.96 ‰. At the top of the sec-
tion, the limestones of the Middle Eocene display slightly
negative
δ
13
C values (facies 11; —0.66 ‰ and —0.56 ‰ respec-
tively in samples M211 and M211/1).
The
δ
18
O curve for this section shows very similar varia-
tions to the
δ
13
C curve. Two main features of the
δ
18
O record
are observed in the Late Cretaceous: (1) the negative excur-
sion with the lowest value (—3.95 ‰) in sample M109; and (2)
173
METEORIC DIAGENESIS OF CRETACEOUS—EOCENE SHALLOW-WATER CARBONATES (ALBANIA)
Fig. 4. Calcimetry profile for the La Route section (Makareshi massif). Data are listed in Table 1. Legend: Fig. 2. Note: Stratigraphic posi-
tion of grouped samples: I – (M10, M17, M20, M25, M35, M41, M46); II – (M47, M73, M92, M99, M105); III – (M109, M127,
M129, M136, M142, M145, Ms16, M186, M186/1, M159, M171, M172, M174, M177, M179); IV – (M191, M194, M201, M205, M209,
M210, M211, M211/1).
the broad positive excursion followed by values mostly fluctu-
ating around —2.4 ‰. In contrast to the L’Escalier section, the
Middle Eocene limestones (facies 11) display here more nega-
tive values (—3.8 ‰ and —3.71 ‰ respectively in samples
M211 and M211/1), similar to the negative peak identified by
the sample M109.
Rare earth element (REE) measurements
In the L’Escalier section (Fig. 7), normalized REE values of
the Late Cretaceous and the Paleocene limestones fluctuate
between 0 and 0.025, whereas the highest values are recorded
in the Middle Eocene limestones ranging from 0.019 to 0.058:
normalized REE positive peaks (marked by black arrows) are
distinguished in samples V45, V60,V91, V146, V194 and
V207.
Normalized REE variations in the La Route section (Fig. 8)
are less pronounced than in the other section. But during the
Late Cretaceous time, a significant positive peak (sample 109)
was recorded near the top of the CsB5 Biozone.
Interpretation of geochemical variations and
discussion
Diagenetic effects on the trace elements and the isotopic sig-
nature
The strontium profiles for the Cretaceous carbonates of the
L’Escalier section, corresponding to the CsB4 and CsB5 Bio-
zones (samples V36 to V178; Fig. 5, Table 2) and for the en-
tire La Route section (Fig. 6, Table 2), display depleted values
between 200 and 400 ppm. They are very low in comparison
with global values of Cretaceous pelagic limestones (500—
900 ppm; Steuber 2002) and of Carboniferous micrites (700 to
3400 ppm; Wiggins 1986), which are interpreted and consid-
ered as initial marine values of carbonate sediment (Wiggins
1986; Steuber & Veizer 2002). Similar depleted values (rang-
ing from 200 to 400 ppm) have been reported in the Bajocian-
Bathonian and Middle Oxfordian carbonate-shelf sedimentary
successions of the Paris Basin (France), (Vincent et al. 1997,
2006). According to Vincent et al. (2006) low strontium con-
tents can be explained by the meteoric water-rock interactions
involving freshwater fluids with very low Sr and Mg contents
during burial diagenesis.
Bulk carbonates from the various depositional environ-
ments of the two sections show no significant differences in
the oxygen isotope ratios (Figs. 5 and 6, Table 2). These val-
ues are relatively homogeneous, around —2.90 ‰ in the La
Route section and —3.56 ‰ in the L’Escalier section. All these
data might be interpreted as a result of diagenetic stabilization
of the carbonate mud in an “open water-buffered oxygen sys-
tem” (Joachimski 1994). During early diagenesis meteoric
waters migrate through pore spaces, thus allowing chemical
interactions between the water and rock constituents. In this
way, the isotopically lighter meteoric water can overprint the
carbonates, leaving a more depleted signature than the prima-
ry signature of deposition.
Petrographic observations have shown some valuable indi-
cations proving several phases of diagenesis: (a) early diagen-
esis as proved by the presence of crystals of dolomite scattered
174
HEBA, PRICHONNET and EL ALBANI
Fig. 5.
Strontium and stable isotope
profiles for the L’Escalier secti
on (Kruje-Dajt massif). Data are
listed in Table 2. Legend: Fig
. 2.
in calcite matrix, partially recrys-
tallized; (b) early to later diagene-
sis as proved by a coarse cement
filling the residual porosity; and
(c) late (burial ?) diagenesis as
demonstrated by three stages of
recrystallization in calcite veins
(centripetal zonation: black, yel-
low and yellow-orange), as shown
by cathodoluminescence analysis
(thin section V163, L’Escalier
section, Table 2) (Heba 1997).
In
both
studied
sections
(Figs. 5 and 6, Table 2),
δ
13
C and
δ
18
O appear to change in parallel.
In carbonate platforms, positive
covariance between
δ
13
C and
δ
18
O has been interpreted as a re-
sult of early diagenetic alteration
of limestones in the marine-mete-
oric mixing zone (Joachimski
1994; Buonocunto et al. 2002; Al-
lan & Matthews 2006). In the
Kruja Platform, cross-plots of
δ
18
O vs.
δ
13
C values (Fig. 9) show
a covariant isotopic trend for the
La Route section (Fig. 9B) that is
indicative of a clear diagenetic
alteration, and a minor covaria-
tion for the L’Escalier section
(Fig. 9A), suggesting a weaker di-
agenetic alteration.
In particular, isotope values de-
crease towards levels defined re-
spectively by sample V178 in the
L’Escalier section (
δ
13
C=—0.44 ‰
and
δ
18
O= — 4.93 ‰) and sample
M109 in the La Route section
(
δ
13
C= — 4.30 ‰,
δ
18
O= — 3.95 ‰).
These negative peaks are followed
in the two sections by sharp posi-
tive shifts in
δ
13
C and
δ
18
O val-
ues. Moreover, the negative
δ
13
C
and
δ
18
O values at the level of
sample V178 in the L’Escalier
section correspond to the end of
the low Sr values (e.g. 200 to
400 ppm, Fig. 5), whereas in the
La Route section, the negative
isotopic peaks at the level of sam-
ple M109 correspond to the low
value of Sr (e.g. 118 ppm, Fig. 6)
and the positive peak in the nor-
malized REE profile (Fig. 8). All
these data seem to indicate sub-
aerial exposure near the level of
sample V178 in the L’Escalier
section and near the level of sam-
ple M109 in the La Route section.
175
METEORIC DIAGENESIS OF CRETACEOUS—EOCENE SHALLOW-WATER CARBONATES (ALBANIA)
Fig. 6.
Strontium
and
stable
isotope
profiles
for
the
La
Route
section
(Makareshi
massif).
Data
are
listed
in
Table 2.
Legend:
Fig. 2
.
According to Joachimski (1994) and Buonocunto et al.
(2002) the record of this kind of subaerial exposure, in
both sections here, is related to soil-derived influence in
δ
13
C values and to meteoric diagenesis effect in
δ
18
O and
Sr values. The positive peak in the normalized REE pro-
file of the La Route section (sample M109, Fig. 8) may
result from a probable weak pedogenetic influence near
the exposed surface in this section and to an increase of
detrital input during the transgressive phase of the S1 cy-
cle (genetic sequence).
Geochemical patterns as indicators of system tracts and
depositional environments
In the L’Escalier section, the exposure event at the lev-
el of sample V178 indicated by the end of the low values
of Sr content and the decreasing trend of isotopic signa-
tures (Fig. 5), corresponds to the transgressive surface of
the progradational parasequence set of the S11 cycle
(Heba & Prichonnet 2006). This semi-regression cycle
characterized by the upper intertidal to supratidal envi-
ronments (facies 7 and 8, Fig. 2) was followed by a sharp
deepening of the environment (facies 4) that coincides
with sharply rising Sr,
δ
13
C and
δ
18
O values. The subaeri-
al event recorded in the La Route section (at the level of
sample M109) by the low Sr content and the low
δ
13
C
and
δ
18
O values (Fig. 6), and the positive peak on the
normalized REE (Fig. 8) is consistent with the sedimen-
tological interpretation (Heba & Prichonnet 2006): this
event registered near a transgressive surface coincides
with the inflection point between the progradational
parasequence set of the S1 cycle (intertidal environment,
facies 1 and 2, Fig. 2) and the facies 5 wich indicates a
relatively deeper environment (subtidal).
In the two sections, these subaerial events are regis-
tered at the same stratigraphic position, between Bio-
zones CsB5 (Early Campanian) and CsB6 (Late
Campanian—Early Maastrichtian), at the regressive sys-
tem tract (S11 in the L’Escalier and S1 in the La Route).
That suggests a local maximum of the regression in the
Kruja Platform. A similar episode of exposure is recog-
nized at the same time during the late Middle Campanian
(77.3 Ma) in the Island of Brač carbonate platform
(Apulia domain, in Croatia) by decreasing strontium iso-
tope values of low-Mg calcite of rudist shells (Steuber et
al. 2005). This correlation reflects a larger inter-regional
feature: all these platforms of the Apulia domain
emerged at the same time. Moreover, this phenomenon is
correlated with the global
sea-level fall reported from the
Boreal Realm, North Atlantic, and the southern Tethyan
margin (Jarvis et al. 2002; Steuber et al. 2005). This evi-
dence strongly suggests that the CsB5 sedimentation in
the two sections was eustatically controlled and another
maximum regression may have occurred at the transition
between the CsB5 and CsB6 Biozones, a biostratigraphic
limit (named the New Exposure in Figs. 5, 6 and 8).
The variations in Sr contents are known to reflect the
paleosalinity of the seawater in which carbonates precipi-
tate with increasing Sr contents reflecting increasing sa-
176
HEBA, PRICHONNET and EL ALBANI
Fig. 7. Normalized Rare Earth Elements (REE) profiles for the L’Escalier section (Kruje-Dajt massif). Data are listed in Table 4. Legend:
Fig. 2. Note: Solid arrows indicate positive geochemical tendency.
linity (Steuber & Veizer 2002). In carbonate platforms, a
high Sr content reflects a more open marine environment lo-
cated in the distal part of a depositional profile and, inverse-
ly, a low Sr content is indicative of a low salinity
environment near subaerially exposed islands, located in the
proximal part of the same profile (Vincent et al. 2006). As a
matter of fact, in both sections of the Kruja Platform, petro-
graphic observation did not allow us to find any kind of
evaporite precipitation (crystals or ghost crystals of gypsum
or anhydrite). The highest contents of Sr (765.25 and
1016.68 ppm, Table 2) in the L’Escalier section (samples
V204 and V207, Fig. 5) are associated with nummulites and
discocyclines limestones (facies 11) of Middle Eocene age
(Heba & Prichonnet 2006): this is new evidence reflecting
open marine conditions with normal salinity and characteriz-
ing more distal depositional environment of facies 11
(Fig. 2). In contrast, the low Sr contents recorded by the
same facies in the La Route section and by all proximal dep-
ositional environments (facies 1 to 9) which characterize the
Upper Cretaceous carbonates in the two sections may indi-
cate the influence of meteoric water (low salinity) due to the
decrease in paleobathymetry and the exposure related to ear-
ly diagenesis, and the effects of burial diagenesis (Vincent et
al. 1997, 2006), as discussed in section 5.1.
Normalized REE variations are more significant in the
L’Escalier section (Fig. 7) than in the La Route section. The
highest values (black arrows, samples V45, V91, V146,
V194 and V207) correspond to the retrogradational parase-
quence set (sequences S3, S5, S8, S12, S14) and suggest a
series of short and more important detrital inputs that charac-
terize transgressive systems tracts. However, some anoma-
lies are observed during the regressive episodes of three
sequences: high REE values in the sequence S4 (sample
V61); and high lanthanum values in the sequences S7 (sam-
ple V110) and S11 (sample V178). These deviations from the
predicted relationships suggest perturbations in the local clay
input included in the insoluble fraction of calcimeter analyses
which has been controlled in 4 samples, showing proportions
of up to 12 % of insoluble material (Figs. 3 and 4): samples
V173, V187, M73 and M136.
177
METEORIC DIAGENESIS OF CRETACEOUS—EOCENE SHALLOW-WATER CARBONATES (ALBANIA)
Fig. 8. Normalized Rare Earth Elements (REE) profiles for the La Route section (Makareshi massif). Data are listed in Table 4. Legend:
Figs. 2 and 8.
Fig. 9. Cross-plot of
δ
13
C and
δ
18
O values of measured bulk sedi-
ment samples for: A – L’Escalier section (Kruje-Dajt massif); and
B – La Route section (Makareshi massif). Regression analysis of
δ
13
C and
δ
18
O (thick lines), equations and correlation coefficients
(r
2
values) are noted. Data are listed in Table 2.
In the two sections, peaks in dolomite content are isolated
between the limestone facies. Several peaks correspond to the
progradational set of genetic sequence: S2, S3 and S11 se-
quences in the L’Escalier section (Fig. 3); and S2, S4 and S6
sequences in the La Route section (Fig. 4). Moreover, near the
top of these sections, the dolomite increase (samples V203 in
L’Escalier and M210 in La Route) coincides with the major
regression in the Kruja Platform at the end of the Early Maas-
trichtian time recorded in the S13 and S6 sequences, which in-
clude essentially upper intertidal to supratidal environments
(facies 7 and 8, Fig. 2). Finally, in the L’Escalier section, two
peaks in dolomite content (samples V2 and V3, Fig. 3) are as-
sociated with dolomite facies, such as brecciated dolomites
(facies 9) and bioturbated dolomite (facies 5). This distribu-
tion of high values in the dolomite content in both sections
supports the sebkha-type dolomitization in a very shallow en-
vironment (Heba & Prichonnet 2006).
Conclusions
The study of the geochemical signatures together with sedi-
mentological data of shallow-water carbonates of Late Creta-
ceous and Paleocene to Middle Eocene age from the
L’Escalier (Kruje-Dajt massif) and La Route (Makareshi mas-
sif) sections, Kruja Platform (Albania), supports the following
conclusions:
1 – The depleted values in strontium contents (most of
them, from 200 to 400 ppm), the homogeneous
δ
18
O values
(between —2.90 ‰ and —3.56 ‰) in the two sections and the
significant covariation between
δ
13
C and
δ
18
O in the La Route
section reflect the development of a regional meteoric phase
and associated carbonate diagenesis. Consequently, the initial
marine chemical signal is modified during the diagenesis de-
178
HEBA, PRICHONNET and EL ALBANI
veloped near subaerial-exposed sedimentary environments.
Petrographic analyses support these results;
2 – The geochemical patterns suggest a new exposure lev-
el during the Late Cretaceous time, at the CsB5/CsB6 bios-
tratigraphic limit. In the L’Escalier section, this exposure
recorded by sample V178 is identified by the end of the low Sr
values and by the negative excursions of
δ
13
C and
δ
18
O val-
ues. In the La Route section, the exposure level recorded by
sample M109 is characterized by the low Sr values and by the
low
δ
13
C and
δ
18
O values, and the positive peak of normalized
REE values. This subaerial exposure, at the end of the regres-
sive phase of the S11 sequence (L’Escalier section) and the S1
sequence (La Route section), is comparable to that recognized
by the decrease of strontium isotope values of rudist shells in
the Island of Brač (Apulia domain). It could correspond to the
global
sea-level reported from the Boreal Realm, North Atlan-
tic and the southern Tethyan margin;
3 – The high Sr content in samples V204 (780 ppm) and
V207 (1016 ppm) in Middle Eocene carbonates (facies 11,
nummulites and discocyclines limestones) at the L’Escalier
section probably reflects a more distal part of the Kruja Plat-
form during this time, in a normal open marine environment;
4 – Elevated values for REE in both sections coincide with
maximum water depths during the transgression episode.
Anomalies in REE concentrations during regressive episodes
in sequences S4, S7 and S11 in the La Route section suggest
local perturbations possibly linked with a small increase in
clay content, but more data would be necessary to decipher the
exact origin of these changes;
5 – The increase in dolomite contents (55—86 %) corre-
sponds to the regressive episodes in genetic sequences and do-
lomitic facies, suggesting a sebkha-type dolomitization as
explained by the sedimentological analysis.
The geochemical characterization therefore appears to be a
useful approach to complete the general environment of plat-
form sedimentation in an emersion context. A comparison of
these results with data from equivalent platforms in the Apulia
domain would be of interest.
Acknowledgments: Funding was provided by the UQAM (to
the first author) and from the Agence Universitaire de la Fran-
cophonie (AUF) through a project conducted by the second
author. We thank Benoit Vincent for his criticism of a prelimi-
nary draft and useful suggestions. We would like to thank
François Hamel for his help during calcimetry measurements,
Jennifer McKay and Bassam Ghaleb for assistance respective-
ly with stable isotope analysis and REE. We thank Ross
Stevenson and Alain Meunier for their useful comments, and
Pierre-Simon Ross for his help in the translation of an early
draft. We also thank Corinne Loisy, Artan Tashko and one
anonymous reviewer for constructive reviews and the im-
provement of this paper.
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