Ore Geology Reviews 72 (2016) 1072–1087

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Ore Geology Reviews

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The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (OrientalHigh Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

Larbi Rddad a,⁎, Salah Bouhlel b

a Kingsborough Community College of the City University of New York, Department of Physical Sciences, Earth and Planetary Division, department of Physical Sciences, 2001 Oriental Boulevard,Brooklyn, New York, NY 11235-2398, USAb UR11ES16, Earth Sciences Department, Faculty of Sciences of Tunis, University Tunis El Manar, 2092 Tunis, Tunisia

⁎ Corresponding author.E-mail address: Lrddad@gmail.com (L. Rddad).

http://dx.doi.org/10.1016/j.oregeorev.2015.08.0110169-1368/Published by Elsevier B.V.

a b s t r a c t

a r t i c l e i n f o

Article history:Received 7 April 2015Received in revised form 14 August 2015Accepted 18 August 2015Available online 28 August 2015

Keywords:MVT Pb–Zn–BaFluid inclusionsC–O–S–Pb isotopesOriental High AtlasMorocco

The Bou Dahar Pb–Zn–Ba (±Sr) is hosted in the Lower and Middle Liassic carbonate platform in the orientalHigh Atlas of Morocco. The paragenetic sequence includes quartz–pyrite–melnicovite–sphalerite–galena–calcite–barite ± fluorite– ± celestite. Fluid-inclusion studies were conducted on sphalerite (early mineralizingstage) and barite, and celestite (late mineralizing stage). These studies reveal two end-member fluids, a hot(~143 °C) and saline fluid (~23 wt.% NaCl eq.) and a cooler (b50 °C) and diluted fluid (~5 wt.% NaCl eq.).Based on fluid-inclusion and C–O–S isotope studies, a conclusion is reached that the Bou Dahar ore depositswere formed by themixing of two fluid— a diluted, SO2−

4-rich fluid, and an 18O-enriched basinal brine that car-ried Pb, Zn, and Ba. The sulfur required for the precipitation of sulfideswas generated by the thermochemical sul-fate reduction of dissolved sulfate (SO4

2−) of the Mesozoic seawaters, and delivered to the site of ore deposition.The sulfur of sulfatemineralswas derived directly from these dissolved SO4

2. The Pb isotope compositions are ho-mogenouswith 206Pb/204Pb, 207Pb/204Pb, and 208Pb/204Pb ratios ranging from 18.124 to 18.183, 15.630 to 15.634,and 38.325 to 38.440 respectively. This Pb isotope composition is indicative of an upper crust and orogene reser-voirs as the source of lead and other metals. The emplacement of mineralization occurred during the Eocene–Miocene Alpine orogeny, and tectonic burial and compression were the driving forces behind the circulation ofthe orogenic-brines. These ore-forming fluids migrated, along thrusting regional E–W and NE–SW deep-seatedfaults, to the confined carbonate-Liassic reservoir.

Published by Elsevier B.V.

1. Introduction

The Bou Dahar Pb–Zn–Ba district, an ENE–WSW-trending plateauextending over about 40 km, is located in the oriental High AtlasMoun-tains of Morocco 150 km west from the city of Rich (Fig. 1). It is one ofthe most important districts in the oriental High Atlas, and is similarin economic value to the Touissit–Bou Beker district, located in the “laChaîne-des-Horsts” Atlasic belt in northeastern Morocco. The BouDahar ore deposits, with sulfide and non-sulfide ores, were discoveredin 1911 and were exploited by the mining company of Guir (la SociétéMinière du Haut Guir) from 1924 to 1955. In 1955, the Mining andMetallurgical Company (SociétéMinière etmétallurgique) of Peñarroyatook over the exploitation of the district until 1958. Afterward, local ar-tisanal miners have been permitted to exploit these mines with the as-sistance of The Central for Purchasing and Development of the MiningRegion of Tafilalet and Figuig (la Centrale d'Achat et de Développementde la région minière de Tafilalet et de Figuig (CADETAF)). The totalproduction is estimated at 400,000 tonnes of ore grading from 17% to47% Zn and 40% to 70% Pb. The Zn is mainly extracted from the zinc

oxides (calamine). The production of barite, mined mainly fromTaboudaharte deposit, is estimated at 220.000 tonnes

Based on mapping and broad mineralogical descriptions, some re-searchers proposed that the genesis of the Bou Dahar ore deposits wasrelated to the mobilization of deep fluids of magmatic or brine duringthe post-Cretaceous tectonic phase that formed the Atlas mountains(Agard and Du Dresnay, 1965; Le Blanc, 1968; Bazin, 1968; Rddadet al., 1995). Bazin (1968) investigated the Tizi-n'Firest ore deposits, inparticular the Karstic ore deposits hosted in Lower reef limestone, andproposed an epigenetic origin for some ores and syngenetic for others.Le Blanc (1968) proposed an epigenetic origin for the Bou Arhous Pb–Zn ores which are hosted in Lower and Middle Liassic limestone. Caïa(1968) investigated the Tirrhist Pb–Zn ore deposit, and proposed thatthe genesis of themineralizationwas related to the post-Jurassic tecton-ic movement.

Later on, microthermometric data were obtained from sphalerite ofToutia, Corne Wast, Chitane, and Yacoub; from barite of Taboudaharte;and from celestite of Rich-Khole (Rddad and Bouhlel, 1997; Rddad,1998), and later from sphalerite and calcite (Adil et al., 2004). Themicrothermometric results revealed that the mixing of two differentfluids was responsible for the mineralization (Rddad and Bouhlel,1997; Rddad, 1998; Adil et al., 2004). Using Cl/Br halogen, Adil et al.

Fig. 1. General location of the Bou Dahar in the Moroccan Oriental High Atlas.

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(2004) concluded that the mineralizing fluid acquired its high salinitymainly from evaporated seawater.

The sources and interrelationships of the ore-forming fluids, thesources and mode of migration of metals and sulfur, as well as thetiming of ore deposition remain poorly constrained. The present paperaims at reaching a more comprehensive understanding of the physico-chemical nature and sources of the fluids involved in the genesis ofthe Bou Dahar Pb–Zn–Ba (±Sr) ore district. It also provides an insightinto a broader ore genesis at the High Atlas metallogenic province. To

that end, this work combines ore petrography, mineralogy, stable(S, C, O) and radiogenic (Pb) isotope studies, microthermometry offluid inclusions data.

2. Regional geologic setting and Zn–Pb ore deposits distribution

The Atlas Mountains extend from Morocco to Tunisia with signifi-cant lateral variations of altitudes. The Moroccan segment of the Atlasincludes the Middle Atlas to the north and the High Atlas in central

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Morocco. The High Atlas is bounded by the Variscan Meseta and theHigh Plateau to the north, and the Precambrian Anti-Atlas massif withits Paleozoic cover to the south (Fig. 1). It consists of Mesozoic to Ceno-zoic sedimentary rocks covering a Precambrian to Paleozoic basementwhich was deformed by the Hercynian orogeny (Piqué and Michard,1989). The Paleozoic succession, composed mainly of siliclastic rocks,outcrops in Mouguer and Tamlet inliers. The regional Paleozoic sectionof the High Atlas consists of Cambro-Ordovician facies (schist andquartzite), and the Silurian facies (phtanites, schist, and graptolites)(Du Dresnay, 1975).

The High Atlas region underwent the Triassic rifting which wasrelated to the opening of the central Atlantic Ocean and the formationof the Tethys Ocean (Laville, 1988; Giese and Jacobshagen, 1992). TheHercynian NE–SW-trending faults, entrenched in the Paleozoic base-ment, were reactivated (Laville, 1985) and led to the formation of theTriassic rift basins. These basins received detrital clastic rocks and evap-orates interbeddedwith thoelitic and doleritic flows (DuDresnay, 1987;Thane et al., 1983). The Lower Liassic carbonate platform, overlappingthe Triassic series, was developed and upgraded into marls alternatingwith turbiditic limestone (Du Dresnay, 1979). This change in sedimen-tation was related to the Middle Liassic–Middle Jurassic rifting(Warme, 1988). At the end of the Middle Jurassic, a regional upliftoccurred (Saddiqi et al., 2009) and a marine regression led to thedeposition of continental red beds (Jenny et al., 1981; Charrière et al.,2005).

Tectonic inversion due to the convergence between the African andEuropean plates started toward the end of the Cretaceous period(Tapponier, 1977; Olivet, 1978). Successive compression eventsoccurred during the Cenozoic and Quaternary (Laville et al., 1977;Laville, 1985). The first tectonic Atlasic event occurred during theMiddle–Late Eocene, followed by a quiescent period during the Oligo–Miocene (Frizon de Lamotte et al., 2009). The second shortening Atlasicevent, responsible for the uplift and the formation of the High Atlas,took place during the Late Miocene–Pliocene (Frizon de Lamotte et al.,2009). The tectonic model responsible for the formation of theMoroccan High Atlas is predominantly a thick-skinned model whichinvolved the Hercynian faults, the Paleozoic basement structures,and the Mesozoic–Cretaceous cover (Teixell et al., 2003).

The Moroccan High Atlas Zn–Pb ore deposits constitute an impor-tant metallogenic province with several prospects and ore districts(Ovtracht, 1978). It is part of the Zn–Pb province of the circum-Mediterranean Sea and the Alpine Europe (e.g. Rouvier et al., 1985;Bouhlel, 2005). The ore deposits are located in the borders of the HighAtlas and near the paleohighs (e.g., Mougueur, Bou Dahar). Accordingto Mouguina (2004), the High Atlas ore deposits are distributed in twomain stratigraphic levels as follows:

• The Lower Jurassic (Lias) — The ore deposits, hosted in the LowerJurassic, are strata-bound. They consist of numerous lens-shapedZn–Pb–Fe sulfide orebodies, and are considered to be of syngeneticorigin (Agard and Du Dresnay, 1965; Emberger, 1965; Bazin, 1968;Auajjar and Boulègue, 1999).

• TheMiddle Jurassic (Dogger)— The ore deposits, hosted in theMiddleJurassic, are carbonate-hosted Pb–Zn deposits related to the emplace-ment of magmas. The Pb–Zn ore is mainly disseminated in gabbro,with an early Cu–Ni mineralization (Chèvremont, 1975) and a laterZn–Pb hydrothermal episode (Caïa, 1968). On the basis of structuraland mineralogical studies, Mouguina and Daoudi (2008) have pro-posed, however, that some of the Middle Jurassic Zn–Pb ore depositsof the High Atlas are similar to the ones described in the High plateauzone (e.g., Touissit and Mibladen) (Dagallier, 1977; Wadjinny, 1989;Bouabdellah et al., 2012), and probably also to the Eastern HighAtlas Pb–Zn–Cu ore deposits described by Rajlich et al. (1983). ForTouissit-Bou Beker, for example, the Pb–Zn mineralization was de-scribed as MVT ore deposits hosted in the Aalenian–Bajocian carbon-ate platform.According to Bouabdellah et al. (2012),metals in the ore-

bearing fluids were sourced from the Visean rhyodacites andvolcaniclastic rocks, and the ore emplacement took place during theMiocene Alpine orogeny.

The present study of the Bou Dahar district provides a broaderunderstanding of the origin of ore-forming fluids and the genesis ofcarbonate-hosted Pb–Zn–Ba ore deposits in the High Atlasmetallogenicprovince.

3. Geology of Jebel Bou Dahar district

The Bou Dahar structure, rock ages and lithologies are presented inFig. 2. The Bou Dahar is a flat anticline striking ENE–WSW, 40 km longand 15 km wide plateau which lies near the central part of the EasternHigh Atlas (Fig. 1). It is located about 15 km to thewest of the PaleozoicTamlelt Massif. The Bou Dahar Jurassic plateau corresponds to a pre-served Pliensbachian coral reef and carbonate platforms (Agard andDu Dresnay, 1965). While a Paleozoic paleorelief crops out in the foldedcentral part of the Jebel Bou Dahar, the southern domain rather displaysa tabular architecture that is marked by a rim of coral-rich limestonesurrounding thin-bedded limestone originally formed in a lagoon(Agard and Du Dresnay, 1965).

The Paleozoic facies of Cambrian–Silurian age (Agard and DuDresnay, 1965) outcrops in the core of the Bou Dahar fold, and is wellexposed in the Sebbab Kebir area where it forms an E–W oriented out-crop that is 12 km long and about 2 kmwide (Fig. 2a). It consists of thickfolded series of schists alternating with quartzite, dipping 15° to 20° tothe north. The Paleozoic was affected by numerous E–W- to NE–SW-trending faults. Locally, it was intruded bymicrogabbro dikesmost like-ly of Triassic age.

The Triassic formation consists of deformed red beds and basalticrocks where the evaporate component may have been dissolved at ornear the surface. This formation is transgressive, in discordance D0,over the Paleozoic basement (Fig. 2b). The Jurassic succession, whichforms most of the Jebel Bou Dahar, was studied by Agard and DuDresnay (1965), Crevello (1990), Campbell and Stafleu (1992), Rddad(1998), Della Porta et al. (2012) amongothers. The following six Jurassicunits (from the base upwards) were distinguished (Fig. 2b and c):

Unit 1 (10–50m)— thick laminated stromatolitic dolomite strata ofLower Sinemurian age, transgressive over the Triassic rocks.

Unit 2 (~200 m) — oolitic limestone beds, locally silicified, ofMiddle–Late Sinemurian, intercalated with red marls. Units 1 and 2form the Lower Liassic carbonate platform which hosts the strata-bound Pb–Zn ore deposits.Unit 3 (10–50m)— thinmarlstone beds of Carixian age, overlappingthe oolitic limestone.Unit 4 (~200m)—massive bioclastic and reef limestone forming thePliensbachian carbonate platform, locally silicified and dolomitized.This unit is the host of the vein-type Pb–Zn ore deposits.Unit 5 (~200 m) — Toarcian marls and Aalenian black mudstonesthat progressively onlap the Pliensbachian platform flanks, andoverlie the top platform. This indicates the abrupt cessation of car-bonate platform evolution at the Domerian–Toarcian transition(Du Dresnay, 1975; Crevello, 1990; Campbell and Stafleu, 1992).The Aalenian black mudstones locally filled synsedimentary frac-tures within the upper part of the Pliensbachian limestones(Rddad, 1998).Unit 6 (N500m)— deepmarine basin shales andmarlswith few thinbeds of limestone of the Bajocian age (termed the Talsint Marls).They overlay the Toarcian and Aalenian shales and mudstones.

Units 1 and 2,which form the Lower Liassic carbonate, are composedof shallow marine-type carbonate that developed on an active marine

Fig. 2.Geologyof the BouDahar district. a: Geologicmap showingdifferent lithologies. b: Lithostratigraphic column (D0, D1, D2, D3: Unconformities), and c: the cross-section along lineA–Bin Fig. 2a. Key for ages and lithologies are shown in Fig. 2a.

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rift basin (Della Porta et al., 2012). During the Late Sinemurian, block-faulting activities uplifted the Paleozoic basement along Sebbab Kebirforming a paleohigh. The Bou Dahar platform evolved from a low-relief ramp to a high-relief ramp (Della Porta et al., 2012) on whichthe Middle Liassic carbonate (Unit 3) was developed. The block-faulting activities, caused by the overall E–W-trending normal faults,led to the differentiation of four distinct paleogeographic domains thatare from north to south: (i) the Talsint basin; (ii) the Sebbab Kebirpaleohigh; (iii) the Pliensbachian carbonate platform and (iv) thedeep Beni Bassia basin.

The Domerian–Toarcian transition period was marked by a majorextensional tectonic activity resulting from the reactivation of E–Wand NE–SW striking faults. This activity segmented, fractured, anddrowned the Bou Dahar carbonate platforms. These platforms werelater sealed by the Toarcian and Aalenain shales and marlstones. Atthe margins of the Bou Dahar platform, the sedimentation consists ofalternating beds of marls and argillaceous limestones, indicating a rela-tively deep marine environment maintained during the Bajocian (DuDresnay, 1975).

The Jurassic tectonic activities caused three disconformities in theJurassic succession (Fig. 2b) (Agard andDuDresnay, 1965). The first dis-conformity (D1) along with the local conglomeratic layers developedbetween unit 1 and unit 2. The second (D2) and third (D3) disconfor-mities developed at the boundary between unit 2 and unit 3, and be-tween unit 4 and unit 5 respectively.

The Alpine orogeny of the late Cretaceous–Miocene caused the in-version of the E–W- to NE–SW-trending faults, and the uplift of thepresent day Bou Dahar plateau.

4. Mineralization and paragenetic sequence

The Bou Dahar district containsmore than thirty Pb–Zn ore depositsand numerous small showings hosted in the Liassic limestone (Fig. 2a).The ore deposits are concentrated along the rims of the Bou Dahar pla-teau, and also around the Sebbab–Kebir Paleozoic paleohigh. Currently,thirty deposits are mined for sulfides and non-sulfide Pb–Zn ores. Mostof them are located in the western area of the plateau (Fig. 2).

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The description of the orebodies led to the distinction between low-grade, strata-bound andmassive, high-grade, vein-type ores (Agard andDuDresnay, 1965; Rddad, 1998).Most of the ore zones followed E–WtoNE–SW trends parallel to the structural trend of the BouDahar anticline.Mineralization is hosted in two stratigraphic units: the Lower Liassic(Sinemurian) oolitic limestone, and the Middle Liassic (Pliensbachian)bioclastic and reef limestone.

The Sinemurian-hosted ore forms discontinuous, strata-bound, lens-shaped orebodies 20 to 30 m thick (Agard and Du Dresnay, 1965). Theores cemented fractured and brecciated limestone strata, and formedENE–SSW-trending mineralized zones parallel to the regional faults.Two mineralization styles with similar paragenetic sequences are iden-tified: (i) irregular disseminations of small galena crystals (~0.2 cm)(Fig. 3a) and euhedral sphalerite crystals (up to 15 mm), and (ii)

Fig. 3. Some underground views and some hand samples from the Bou Dahar ore district. a: Disgalena crystals disseminations in limestone (Sebbab). b: Vein filled with massive galena (Gn)sphalerite (Sp) hosted in limestone (Corne Wast). d: Green-colored sphalerite crystals (Sp) cecalcite (Cte1) (Yacoub). f: Honey red and green sphalerite (Sp) cemented by post-ore calcite (Cis referred to the web version of this article.)

stockwork type in a thin and dense fissures network. Both sulfides re-place bioclasts, pellets, and oolites (Fig. 4a).

The Pliensbachian-hosted mineralization forms numerous parallelveins (Fig. 4b) within E–W- to ENE–WSW-trending faults (e.g., Toutia,Chitane, Yacoub, and Taboudaharte deposits). Fault intersections werethe site of wide dissolution and ore emplacement, and thus representzones of economic interest. The veins' dimensions are variable fromone ore deposit to another, but the average dimensions are 300 m-length and 1 m-width. The total length of the known veins is estimatedat 130 km (Agard and Du Dresnay, 1965). The sulfides, non-sulfide Pb–Zn ores, and barite are exploited over a depth extending from 30 to170 m. Locally, the veins intrude the Aalenian black mudstone fillingsynsedimentary faults that crosscut the Pliensbachian limestone(e.g. Corne Wast deposit).

seminated galena (Gn) in the oolitic limestone. Inset shows limestone hand samples withembedded within calamine masses (cal) hosted in limestone (Lim), (Chitane). c: Massivemented by galena (Gn), then by barite (Brt) (Yacoub). e: Galena cemented by sparry orete2) (Toutia). (For interpretation of the references to color in this figure legend, the reader

Fig. 4. Microscopic characteristics of the ores. a: Galena replacing oolitic limestone (Oo), Sebbab. b: Polygonal pyrite (Py) cemented by sphalerite (Sp), and galena (Gn), Yacoub.c: Sphalerite (Sp) cemented by galena (Ga), and barite (Ba), Yacoub. d: Crystals of quartz (Qz) corroded by sphalerite (Sp) hosted in the Pliensbachian limestone (Lim), Chitane.a: Transmitted light; b to d: reflected light.

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The macroscopic andmicroscopic mineral assemblage is simple andincludes pyrite, melnikovite, sphalerite, galena with tetraedrite inclu-sions, barite, and subordinate celestite. Upon examining the under-ground, a vertical ore zoning is noticed, with sulfides occupying thedeeper zones while the sulfate minerals occupy the shallow zones.

Minor pyrite aggregations occur in both the strata-bound and thevein-type ores as subeuhedral and euhedral crystals, and have a fine-to moderately coarse-grained texture. Pyrite is associated with galenaand sphalerite and occurs locally as inclusions in sphalerite and galena(Fig. 4b). Some iron sulfide occurs as colloform textures typical of themelnicovite associated with pyrite, or as inclusions in both sphaleriteand galena (e.g., Yacoub). Translucent honey- to dark green-colored,cm-sized, sphalerite crystals occur as massive patches within the vein(e.g., Chitane), and as fracture-fillings in the limestone host rock(Fig. 3c). They are also disseminated within the bioclastic limestone.Sphalerite crystals are often cemented by galena (e.g., Toutia, CorneWast, Chitane), or by galena and barite successively (Figs. 3d and 4b)(Yacoub). Relics of sphalerite can be found within calamine. Galena oc-curs as euhedral, coarse-grained, fracture-controlled, massive patchesin veins (Fig. 3b) and in dissolution cavities (e.g., Yacoub, Ksar Moghal).In the wall rocks, galena occurs as disseminated, fine- (100 μm) tocoarse-grained (up to 4 cm) euhedral crystals, and as stockwork-typemineralization. Disseminated galena forms numerous large swarmseach of which is guided by fissures parallel to the regional ENE–WSW-trending faults. Galena and minor sphalerite replace the limestonewithout any dissolution or recrystallization of the host limestone. Atthe microscale level, polished and thin sections show galena replacingoolites, bioclastes, and calcitic cement. Micro-inclusions (50 μm) oftetraedrite are embedded in or coated by galena (e.g., Tighanimine oredeposit). Locally, chalcopyrite forms rare aggregates within the veins(Agard and Du Dresnay, 1965).

Barite postdates sphalerite and galena, and fills either E–W veins(Taboudaharte) or dissolution cavities (Yacoub) (Fig. 3d). Minor celes-tite is observed at Rich-Khole, and occurs as prismatic and fibro-radialcrystals at the center of the vein, and a massive band at the border. Atthe base of the massive celestite is a ferruginous strip that is rich infine-grained quartz. Ore calcite occurs as coarse-grained crystals, andis usually associated with galena and sphalerite (Fig. 3e). It also formsagglomerations in the host rock and fills dissolution cavities. Late

calcite (post-ore calcite) seals the small fractures that affect sphalerite(Fig. 3f).

Thewall–rock alteration, associatedwith the various styles ofminer-alization, consists mainly of silicification (Fig. 4d), and occurs as needlebipyramidal quartz crystals crosscutting oolites, bioclasts, and sparriticcement. Quartz is often engulfed or corroded by the sulfide minerals(Fig. 4d), and represents the pre-ore stage of the mineralizing system.Beside silicification, Agard and Du Dresnay (1965) observed rare dolo-mite replacing the host limestone.

A large portion of the exploited ores corresponds to the non-sulfidesecondary Pb–Zn mineralization studied in detail by Choulet et al.(2014). These supergene minerals formed as a result of the oxidationof sulfides by meteoric water during the last 20 Ma (Choulet et al.,2014). The first abundant oxide assemblage, consisting of calamine(Fig. 3b), developed at the expense of sphalerite. The calamineincludes banded red smithsonite, white hydrozincite, collomorphhemimorphite, and red clays. The second but minor oxide assemblageconsists of a mixture of cerussite, covelite, and iron oxides.

The paragenetic sequence is independent of the ore style and of thehost rock age, and consists of four mineralizing stages/events summa-rized in Table 1. Stage 1 is the sulfide event and consists of pyrite–galena–sphalerite-ore calcite (calcite-1) succession. Stage 2 is the sul-fate event and consists of barite and celestite. Stage 3 corresponds tothe post-ore calcite (calcite-2) that fills small fractures crosscutting sul-fide ores and limestone host rocks. Stage 4 corresponds to the oxidationstage of the sulfide ores.

5. Fluid inclusions

Samples were prepared as standard 200 to 500 μm-thick, doubly-polished wafers. The microthermometric measurements were carriedout at the Department of Earth Sciences, Faculty of Sciences of Tunis,using a Linkam THM600 freezing-heating stage on a Leitz microscope.The system was calibrated using pure CO2 fluid inclusion (−56.6 °C),the freezing point of H2O (0 °C), andmelting points of Merck standards.The precision was ±0.5 °C. Fluid salinity was calculated as weight per-cent NaCl equivalent (wt.% NaCl eq.) using the equation of Bodnar(1993).

Table 1Mineral paragenetic sequence and alteration in the Bou Dahar ore district.

Hydrothermal mineralizing period

MineralPre–ore

stage (S0)Sulfide stage

(S1)Sulfate stage

(S2)Post–ore

stage (S3)Oxidized stage (S4)

QuartzSphaleriteGalenaPyriteMelnicoviteCalcite–1Calcite–2BariteCelestiteCalamineCerusiteCoveliteHematiteGoetithe

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5.1. Petrography

The fluid inclusions are rounded, elongated, and rarely irregular inshape, and have an average size of 30 μm. Fluid inclusion assemblagesof Goldstein and Reynolds (1994) and genetic classification as primary,secondary or pseudosecondary of Roedder (1984) were used to classifyfluid inclusions. Fluid inclusions that are clustered or isolated are con-sidered primary. Fluid inclusions that are aligned and occur as planartrails are considered secondary.

Sphalerite shows primary and secondary fluid-inclusion assem-blages. The primary fluid inclusions (L+ V) are aqueous, two-phase in-clusions, with a liquid/vapor ratio of ~85%, and are either isolated orclustered (Fig. 5a). The secondary fluid inclusions (L + V) are aqueous,two-phase inclusions which occur as trails. These secondary fluid inclu-sions are suspected to have undergone necking-down phenomena.They have a narrow salinity range and a wide range of temperature.Therefore, they are not considered in this study.

Barite and celestite contain liquid, one-phase, primary fluid inclu-sions that are clustered or isolated (Fig. 5b). Because barite and celestiteare susceptible to stretching and/or leakage (Ulrich and Bodnar, 1988),fluid inclusions that are hosted in these sulfate minerals and that shownecking-down or FIAs with inconsistent microthermometric data, arenot considered in this study.

5.2. Microthermometric results

A summary of the microthermometric data derived from the studyof 225 primary fluid inclusions hosted in sphalerite, barite, and celestiteis presented in Table 2.

Primary fluid inclusions in sphalerite have eutectic temperature (Te)in the range of−74.2 and−39.3 °C, far below the eutectic of NaCl–H2O

Fig. 5. Primary fluid inclusions hosted in sulfides and sulfates in the Bou Dahar district. a: Isolatephase (L) fluid inclusions hosted in barite, Taboudaharte.

system (−21.2 °C). This indicates the presence of other salts besideNaCl, such as CaCl2 (Te = −52 °C), MgCl2 (Te = −35 °C), and LiCl(Te = −75 to −78 °C) (e.g., Roedder, 1984; Crawford, 1981; Duboisand Marignac, 1997; Davis et al., 1990). Final ice melting temperature(Tm (ice) ) values range between −30.6 and −11.5 °C, correspondingto a salinity range of 15.6 to 29.7 wt.% NaCl eq. (average ~23 ±0.5 wt.% NaCl eq.) (Fig. 6). Homogenization temperature (Th) valuesvary from 106 to 180 °C (143 °C) (Fig. 7). These microthermometricvalues fall within the range of those measured by Adil et al. (2004).

Thermometric measurements on ore calcite were performed by Adilet al. (2004). The eutectic temperatures of the primary fluid inclusionsrange from −80 to −45 °C, indicating the presence of other solutes inthe fluid. Ice melting temperatures vary between −29 and −12 °C,which yields salinity values in the range of 15 to 29 wt.% NaCl eq.Homogenization temperatures range from 60 to 150 °C.

Barite and celestite show only aqueous, single-phase, primaryfluid inclusions. Eutectic temperatures vary from −52 to −40 °C(average =−46 °C), and from−31 to−24.8 °C (average =−27.9 °C)for barite and celestite respectively. This indicates the presence ofother solutes in the fluid such as Ca2+ and Mg2+. The Tm (ice) valuesrange from −17.7 to −9.7 °C (average = −13.7 °C) for barite, and−4.5 to −1.9 °C (average = −3.2 °C) for celestite. These values yielda salinity range of 13.7 to 19.6 wt.% NaCl eq. (average ~ 17 ± 0.5 wt.%NaCl eq.), and of 3.2 to 7.2 wt.% NaCl eq. (average ~ 5 ± 0.5 wt.% NaCleq.) for barite and celestite respectively (Fig. 6). These single-phasefluid inclusions in both barite and celestite were entrapped at atemperature lower than 50 °C (Th ~ 40 °C).

5.3. Pressure corrections

Pressure corrections are minimal given the fact that the Bou DaharMVT ore deposit would form at pressures lower than 1 kbar (Roedder,1984). However, if a maximum cover of about 1 km is assumed, thepressure corrections to the observed temperatures would be approxi-mately 30 °C (Farrington, 1952; Nwachukwu, 1975) at the time of oreformation.

6. Stable (C, O, S) and lead isotopes

6.1. Sampling and analytical procedures

Thirty ore samples were collected from the vein type anddissolution-cavities type, both hosted in the Pliensbachian limestone(Table 3), spanning the early- and late-stage mineralizing events.Samples were taken from 0 m to 170 m underground mining levelsof the Toutia, Corne Wast, Yacoub, Chitane, Taboudaharte, and Rich-Khole (Fig. 2a).

Mineral separates, for stable and radiogenic isotopes, were carefullycrushed and handpicked under a binocularmicroscope. Carbon, oxygen,

d aqueous (L+ V) fluid inclusion hosted in sphalerite, Toutia. b: Clustered aqueous single-

Table 2Microthermometric data of the primary fluid inclusions in the Bou Dahar ore district.

Location Host mineral Stage Inclusion type Num Tm, ice (°C) Salinity (wt.% NaCl eq.) Th (°C) Th (°C)

Range Mean Range Mean Range Mean

Toutia Sphalerite Stage 1 L + V 45 −25.2 to −15.2 −20.7 19.0–26.2 19.2 142.3–179.9 158.9Corne Wast Sphalerite Stage 1 L + V 30 −23.0 to −20.2 −21.7 22.8–24.7 23.8 125–182.5 172.4Chitane Sphalerite Stage 1 L + V 29 −25.8 to −18.2 −21.6 21.4–26.5 23.7 135–156 139.8Yacoub Sphalerite Stage 1 L + V 56 −30.6 to −11.5 −20.5 15.5–29.7 22.8 106.2–172.7 135.1Taboudaharte Barite Stage 2 L 44 −17.7 to −9.7 −13.0 13.7–19.6 16.9 b50 ~40Rich-Khole Celestite Stage 2 L 21 −4.5 to −1.9 −3.3 3.2–7.2 5.3 b50 ~40

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and sulfur isotopes were performed at the Stable Isotope Ratio MassSpectrometry facility at the Department of Geological Sciences and En-gineering, University of Nevada. Lead isotope analyses were made onNu PlasmaMC–ICP-MS at the Ecole Normale Supérieure in Lyon, France.

For carbon and oxygen isotopes, five samples of Pliensbachian hostlimestone, four samples of calcite, associated with the sulfide stage,fromToutia, CorneWast, and Yacoub, and one sample of post-ore calcitefrom Toutia were analyzed. Oxygen isotopes were also measured forfour barite samples of Yacoub and Taboudharte, and for two celestitesamples of Rich-Khole.

The C–O isotope analyses were carried out using a MicromassMultiPrep preparation device interfaced to a dual inlet MicromassIsoprime stable isotope ratio mass spectrometer, using the phosphoricacid reaction method of McCrea (1950), except that the reaction wasperformed at 90 °C. The carbon isotopic compositions are reported indelta notation (δ13C) relative to VPDP, and the oxygen isotopic compo-sitions are reported in delta notation (δ18O) relative to VPDP andVSMOW. Precision of the analyses is better than ±0.2‰.

Sulfur isotopes were carried out on six sphalerite and eight galenasamples from Toutia, Corne Wast, Chitane, and Yacoub. Sulfur isotopemeasurements were also performed on four barite samples fromYacoub, two barite samples of Taboudaharte, and two celestite samplesof Rich Khole. Sulfur isotope analyses were performed using aEurovector elemental analyzer interfaced to a Micromass isoprime sta-ble isotope ratio mass spectrometer, after the methods of Giesemannet al. (1994) and Grassineau et al. (2001). Vanadium oxide (V2O5) wasadded to sulfate samples as a combustion aid. S-isotopic compositionsin sulfide and sulfate minerals are expressed as δ34S values relative tothe VCDT standard, and O isotopic compositions in sulfates areexpressed as δ18O values relative to the VPDP and VSMOW standard.Reproducibility was ±0.2‰ for sulfur, and ±0.5‰ for oxygen.

Lead isotopemeasurementswere performed on four galena samplesfrom Toutia, Chitane, CorneWast and Yacoub. Every two samples werebracketed using SRM-981. Samples and Standards were corrected formass fractionation using Thallium and an exponential law (Albarèdeet al., 2004). The Pb isotope ratios were normalized to the bracketing

Fig. 6. Frequency of ice melting temperatures derived frommicrothermometric studies ofthe primary fluid inclusions in sphalerite, barite, and celestite from the Bou Dahar district.

values of SRM-981. The 2σ errors on the Tl-corrected NIST 981 values,measured during the period the samples were run, were 0.0017%,0.014%, and 0.045% for 206Pb/204Pb, 207Pb/204Pb, and 208Pb/204Pbrespectively.

6.2. Results

6.2.1. Carbon and oxygen isotopesThe C–O isotopic composition of carbonates and the O isotopic com-

position of sulfates are listed in Table 4 and Fig. 8. The host Liassic(Pliensbachian) limestones have δ13C values ranging from 0.5 to 2.9‰(mean = 1.7‰) (Fig. 8) that are within the range typical of marineJurassic limestone (Veizer andHoefs, 1976; Land, 1980). The δ13C valuesof the ore-calcite, associated with the sulfide mineralization, fluctuatebetween 1.6 and 2.5‰, and that of the post-ore calcite is 0.0‰ (Fig. 8).The δ18O values for the ore-calcite range from 18.4 to 21.6‰(mean = 20‰), and are lower than those of the host limestone(Fig. 8). The post-ore calcite has a δ18O value of 15.4‰ (Fig. 8). Theδ18O values of barite and celestite range from 16.1 to 18.2‰, and 16.1to 17.9‰ respectively (Table 4).

6.2.2. Sulfur isotopesSulfur isotope compositions of sphalerite, galena, barite, and celes-

tite are reported in Table 5 and Fig. 9. The δ34S values for galena andsphalerite range from −4.0 to 6.8‰ (mean = 1.4‰), and from 0.7 to5.0‰ (mean = 2.9‰), respectively. The range of the isotopic composi-tions of sulfides is relatively small when compared to that of mostsediment-hosted deposits. The δ34S values of sulfate minerals reveal arelatively small variation of 17.2 to 20.4‰ (mean = 18.8‰) for barite,and of 15.4 to 15.8‰ (mean = 15.6‰) for celestite (Table 5 and Fig. 9).

The δ34S values show the following trend: δ34SSulfides b δ34SSulfates.When comparing the δ34S values of the sulfide minerals, the trendδ34SGn b δ34SSph is observed for Toutia and Corne Wast ore depositswhile the opposite trend δ34SSph b δ34SGn is observed for Chitane andYacoub ore deposits. A hand specimen with the paragenitic sequence

Fig. 7. Frequency of homogenization temperature derived from microthermometricstudies of the primary fluid inclusions in sphalerite from the Bou Dahar district.

Table 3Description of minerals and rocks analyzed in the Bou Dahar ore district.

Location Description of minerals/rocks analyzed Ore stage

Toutia Sphalerite within the vein First stageGalena within the vein First stageCalcite (calcite-1) associated to sphalerite andgalena

First stage

Calcite (calcite-2) filling small fractures insphalerite

Third stage

Middle Liassic limestoneCorne Wast Sphalerite in small masses and filling the vein First stage

Galena within the vein First stageCalcite (calcite-1) associated to sphalerite andgalena

First stage

Middle Liassic limestoneChitane Massive sphalerite within the vein First stage

Crystalline sphalerite within the host carbonate First stageGalena within the vein First stageCalcite (calcite-1) associated to sphalerite andgalena

First stage

Middle Liassic limestoneYacoub Sphalerite within the vein First stage

Barite cementing small masses of galena andsphalerite

Second stage

Calcite (calcite-1) associated to sphalerite andgalena

First stage

Middle Liassic limestoneTaboudaharte Barite Second stageRich-Khole Celestine hosting inclusions of iron oxides and

fluorineSecond stage

Fig. 8. Plot of δ18O vs. δ13C showing the isotopic composition of the Liassic limestone, hy-drothermal calcite, and post-ore calcite for themain ore deposits of the Bou Dahar district.

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of ZnS→ PbS→ BaSO4 from Yacoub has the following isotopic composi-tion trend of δ34S: ZnS b PbS b BaSO4 (Fig. 10).

6.2.3. Lead isotopesThe Pb isotope compositions of galena samples (n = 5) from Bou

Dahar are presented in Table 6 and plotted in the 208Pb/204Pb vs.206Pb/204Pb (thorogenic diagram) and 207Pb/204Pb vs. 206Pb/204Pb(uranogenic diagram) (Fig. 11). The Pb isotopic compositions of galenafrom the Touissit–Bou Beker MVT district (Bouabdellah et al., 2012) arealso plotted for comparison.

The Pb isotope compositions of the Bou Dahar district ores are ho-mogenous with 206Pb/204Pb, 207Pb/204Pb, and 208Pb/204Pb ratios rangingrespectively from 18.124 to 18.183, 15.630 to 15.634, and 38.325 to38.440. The parameters μ (238U/204Pb) and κ (232Th/238U), and modelage (T) values are calculated using the equations of Albarède et al.(2004). The μ and κ values are homogenous and range from 9.79 to

Table 4Carbon and oxygen isotopes of host rock limestone, ore calcite, post-ore calcite and sulfates.

Sample Location Lithology δ13C(‰, VPD

TOH Toutia Limestone 2.2WH Wast Limestone 2.3YH Yacoub Limestone 2.7ChH Chitane Limestone 2.6ChH2 Chitane Limestone 2.9TOC Toutia Ore calcite 1.6TOC2 Toutia Post-ore calcite 0.0WC Wast Ore calcite 2.2YC Yacoub Ore calcite 2.5YC2 Yacoub Ore calcite 1.9YB2 Yacoub BariteYB3a Yacoub BariteTaB1 Taboudaharte BariteTaB2 Yacoub BariteRCe1 Yacoub CelestineRCe2 Yacoub Celestine

9.80 and from 4.08 to 4.12 respectively. The calculated model age(T) is bracketed between 431 and 470 Ma.

7. Discussion

7.1. Nature of the ore fluids

The homogenization–salinity diagram (Fig. 12) reveals two distinctfluid end members trapped in sphalerite and sulfate minerals. The firstfluid, trapped in sphalerite, is characterized by high salinity (~23 ±0.5 wt.% NaCl eq.) and moderate temperature (average ~143 °C). Thisfluid corresponds to the sulfide-stage event. It is a NaCl–KCl–MgCl2–CaCl2 ± LiCl brine as inferred from measured eutectic temperatures(Te average ~ −60 °C). The second end member fluid, observed inaqueous, one-phase, celestite fluid inclusions, has low salinity(average ~ 5 ± 0.5 wt.% NaCl eq.) and low temperature (b50 °C). Thetemperature and salinity obtained from fluid inclusions at Bou Daharfall within the range of most MVT ore-forming fluids (salinity =15–30 wt.% NaCl eq, temperature = 75 °C–200 °C) (Basuki andSpooner, 2004; Leach et al., 2005).

The temperature values recorded in fluid inclusions at BouDahar ex-ceed values expected for geologically reasonable thermal gradients andestimated stratigraphic burial temperatures. Therefore, these tempera-tures can be explained by either: (i) an unusually high geothermal gra-dient, (ii) advective heat transport from deeper parts of the basin asobserved for many other MVT ore districts (e.g., Touissit–Bou Beker,Bouabdellah et al., 1996; Ozark MVT province, Leach et al., 2010), or

B)δ18O(‰, VPDB)

δ18O(‰, VSMOW)

δ18O fluid

(‰, VSMOW)

−8.0 22.7−5.3 25.5−5.1 25.7−6.5 24.2−6.8 23.9−9.0 21.6 6.41

−15.1 15.4−9.5 21.1 5.91

−12.1 18.4 3.26−7.4 23.3 8.08

−14.4 16.1−13.5 17.0−14.3 16.1−12.3 18.2−14.3 16.1−12.6 17.9

Table 5Sulfur isotope composition of sulfides and sulfates from the Bou Dahar ore district.

Sample Location Mineral δ34S (‰, VCDT)

TOG1 Toutia Galena −4.0TOG2 Toutia Galena −2.0TOS1 Toutia Sphalerite 0.7WG1 Corne Wast Galena 0.7WS1 Corne Wast Sphalerite 2.9WS2 Corne Wast Sphalerite 3.1ChG1 Chitane Galena 6.8ChG2 Chitane Galena 6.7ChS1 Chitane Sphalerite 2.6YG1 Yacoub Galena 4.6YG2 Yacoub Galena 5.7YG3 Yacoub Galena 6.0YS2 Yacoub Sphalerite 3.0YS3 Yacoub Sphalerite 5.0YB2 Yacoub Barite 19.8YB3a Yacoub Barite 20.4YB3b Yacoub Barite 20.4YB3c Yacoub Barite 20.0TaB1 Taboudaharte Barite 17.2TaB2 Taboudaharte Barite 18.1TaB3 Taboudaharte Barite 17.9RCe1 Rich-Khole Celestite 15.4RCe2 Rich-Khole Celestite 15.8

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(iii) the ascent of deeply circulating fluids in basement rocks beneaththe deposits (e.g., Upper Silesia and Irish Midlands; Leach et al., 2010).

The salinity values of the ore-forming fluids at Bou Dahar fall withinthe range of those calculated in the worldwide MVT districts where sa-linity is typically in the range of 10 to 30 wt.% NaCl eq. (Leach et al.,2005; Leach et al., 2010). These fluids have compositions and tempera-tures similar to those of oil-field brines (Sverjensky, 1986). The high sa-linity of these sedimentary basinal brines can be explained by thedissolution of evaporates, incorporation of connate bittern brines, orthe infiltration of evaporated surface waters (Hanor, 1979; Carpenteret al., 1974; Viets et al., 1996). For Bou Dahar, the Na–Cl–Br–Li system-atics of sphalerite-hosted fluid inclusions suggest that the high salinityresulted from evaporated seawater with a contribution of low amountsof halite dissolution (Adil et al., 2004).

The δ18O values of carbonates display a general downward trend inthe following sequence: limestone (22.7 to 25.7‰, average =24.2‰) → ore-calcite (18.4 to 21.6‰, average = 20‰) → post-orecalcite (15.4‰). This trend resembles similar trends that have beenobserved at other MVT deposits (e.g., Frank and Lohmann, 1987;Nesbitt and Muehlenbachs, 1994; Spangenberg et al., 1995) in whichisotopically lighter O is observed in paragenetically late carbonates.Lighter δ18O values of post-ore calcite, relative to the ore-calcite, can

Fig. 9. Histogram distribution of the δ34S values for sphalerite, galena, barite and celestitefrom Bou Dahar district.

be attributed to either an increase in temperature, or the introductionof isotopically lighter fluid.

Using the average δ18O values of the ore calcite, the homogenizationtemperature range of 60 to 180 °C, and the oxygen isotope fractionationequation of Friedman and O'Neil (1977), the calculated δ18O of the fluidvaried between −2.1 and 9.4‰. Such fluid is similar to the basinalbrines of the MVT ore deposits (δ18O of +4 to +10‰) (e.g., McLimans, 1977; Ohmoto, 1986).

The oxygen isotope composition of sulfates (barite and celestite) iscloser to that of Mesozoic seawater sulfate (~10–15‰) (Claypoolet al., 1980). This indicates that these sulfate minerals precipitatedfrom an 18O-enriched, SO4

2−-rich fluid derived fromMesozoic seawater.

7.2. Source of metals

The sources of the metals for sediment-hosted, base-metal depositsare a variety of crustal rocks. No special rock type stood out as a pre-ferred source (Leach et al., 2005). The brines leached the metals fromthe rocks it encountered along their paths of migration.

The galena samples show homogenous Pb isotope compositionswith 206Pb/204Pb, 207Pb/204Pb, and 208Pb/204Pb ratios ranging from18.124 to 18.183, 15.630 to 15.634, and 38.325 to 38.440, respectively.According to the plumbotectonic model of Zartman and Doe (1981),these Pb isotope values plot above the orogene curve in the thorogenic(208Pb/204Pb vs 206Pb/204Pb) diagram, and between the upper crust andthe orogene in the uranogenic (207Pb/204Pb vs 206Pb/204Pb) diagram(Fig. 11). This indicates that lead originated from upper crustal andorogene reservoirs, which is consistent with the geodynamic setting ofthe High Atlas to which the studied district belongs.

The calculated μ (238U/204Pb) and κ (232Th/238U) values are veryhomogenous, clustering tightly between 9.79 and 9.80, and between4.08 and 4.12, respectively. These values further confirm the uppercrustal and orogenic reservoirs as the sources of Pb and other metals.

The calculated model age (T) varies from 431 Ma to 470 Ma, and isolder than the proposed Eocene–Miocene age (refer to the discussionbelow). This abnormal older age, typical of numerousMVT ore deposits,is explained by the delay in Pb in-situ growth. This Pb growth retarda-tion is due to the contribution of a low radiogenic material originatingmost likely from the lower crust and/or the preferential removal ofU during orogenic events.

The Paleozoic series consist mainly of siliciclastics, and thus are asuitable source of metals for the Bou Dahar ore deposits. The presence

Fig. 10. Hand specimen δ34S isotopic composition of sphalerite, galena, and barite inYacoub.

Table 6Lead isotope composition of galena, model age (T), μ, and κ from the Bou Dahar deposits. The age of the host rocks is Pliensbachian. Analytical errors, given as 2σ, are 0.0017%, 0.014%, and0.045% for 206Pb/204Pb, 207Pb/204Pb, and 208Pb/204Pb respectively.

Sample Description Location Pb206/Pb204 Pb207/Pb204 Pb208/Pb204 T (Ma) μ (238U/204Pb) κ (232Th/238U)

YG1 Galena associated with calcite Yacoub 18.12390 15.63113 38.43633 470 9.8039 4.1170YG2 Galena cemented by barite Yacoub 18.17431 15.63235 38.43727 435 9.7951 4.0819CHG Euhedral galena within the vein Chitane 18.18267 15.63314 38.43534 431 9.7961 4.0752TOG Massive galena within the vein Toutia 18.17764 15.63375 38.43965 435 9.7999 4.0814WG1 Massive galena within the vein Corne Wast 18.12730 15.62914 38.42542 464 9.7948 4.1078

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of Li, as inferred from the eutectic temperatures and the high values ofcrush-leachmolar Li/Na ratio (~0.007) in the sphalerite-hosted fluid in-clusions (Adil et al., 2004), suggests that the ore-forming fluidinteracted with the siliciclastic Paleozoic Li-bearing clays/micas(e.g., Banks et al., 2002). The presence of deep-seated E–W- toNE–SW-trending Hercynian faults, entrenched deeply within thePaleozoic basement and remobilized during the Alpine orogeny via athick-skinned tectonic model, further supports the upper crustal originof Pb andothermetals. These deep-seated faults have acted as pathwaysfor the rising fluids from the Paleozoic basement from which metalswere mainly leached and transported to the Liassic carbonate orereservoir.

Compared to other Pb–Zn ore deposits in the Moroccan–Algerian–Tunisian atlas belt, the Pb isotopic values of the Bou Dahar district andthe Pb isotope values of Tigrinine–Taabest district (Rddad and Bouhlel,in preparation),which is located in the CentralHighAtlas, are less radio-genic than thePb–Zn Touisit–Bou Beker ore deposits (Bouabdellah et al.,2012). The less radiogenic character of the Bou Dahar district, comparedto Touisit–Bou Beker, reflects differences in the composition of the un-derlying Paleozoic basement. The latter consists of schist in Bou Daharand of schist with Visean rhyodacites and volcaniclastic rocks inTouisit–Bou Beker. Bouabdellah et al. (2012) proposed that the main

Fig. 11. Plots of 208Pb/204Pb vs. 206Pb/204Pb and 207Pb/204Pb vs. 206Pb/204Pb for the BouDahar ore district. Curves of growth trends for Pb isotope ratios are from theplumbotectonic model of Zartman and Doe (1981). Pb isotopic data from Touissit–BouBeker (Bouabdellah et al., 2012) are also plotted for comparison.

source of Pb originated from these rhyodacites and volcaniclasticrocks. Additionally, the Pb isotopic composition recorded in the BouDahar district and in the Moroccan High Atlas in general, is less radio-genic than that of the Tunisian MVT Pb–Zn districts (Bouhlel, 2005;Bouhlel et al., 2013). These Pb isotopic composition differences betweentheMoroccanAtlas and the Tunisian Atlas reflect differences in the com-position of the underlying Paleozoic Pb reservoir rocks. The least radio-genic reservoir is encountered in Morocco while the more evolved,“live” Pb reservoir is found in Tunisia.

7.3. Source of sulfur

Sulfur isotope values of MVT sulfides throughout the world indicatethat sulfur generated from a variety of crustal sources (Ohmoto and Rye,1979; Sangster, 1990; Leach et al., 2010). Individual deposits or districtscan have one or more possible sources of sulfur that may includesulfate-bearing evaporates, connate seawater, diagenetic sulfides,sulfur-bearing organic material, or H2S reservoir gas (Leach et al.,2010). The ultimate source of the sulfur is seawater sulfate trapped bythe sediments in variousminerals and/or connatewater thatwas subse-quently reduced by one or more processes (Sangster, 1990; Leach et al.,2010).

For Bou Dahar, the δ34S values in celestite and barite, ranging be-tween ~15 and 20‰ (Table 4), fall within the range of Mesozoic seawa-ter sulfate (13–20‰) (e.g., Triassic seawater +11 to 20‰; Jurassicseawater +14 to 18‰) (Fig. 12) (Claypool et al., 1980). The δ34S valuesof barite and celestite are also close to those of Triassic gypsum (13.0 to15.6‰) reported in the Touissit–Bou Beker ore district (Bouabdellahet al., 2012). The most obvious source of sulfur for the Bou Dahar oresis the Triassic sulfates underlying the Jurassic carbonate of theMoroccanHigh Atlas.

The reduced sulfur in sphalerite and galena was derived fromdissolved sulfate through thermochemical sulfate reduction (TSR) orbacterial sulfate reduction (BSR) processes. Beyond this basic point,the geochemical pathways by which reduced sulfur was formed andhow it was introduced into the ore zone remain problematic. BSR

Fig. 12. δ34S vs. δ18O plot showing isotopic composition of barite and celestite. The S–Oisotopic composition is compared to the one of Mesozoic seawaters (Claypool et al.,1980; Veizer et al., 1999).

Fig. 13. Evolution of the mineralizing fluid system at the Bou Dahar ore district.

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takes place under low temperatures, generally below 80 °C (Dixon andDavidson, 1996; Jørgensen et al., 1992; Machel, 1987). Conversely, TSRoccurs via a reaction involving hydrocarbons at a temperature environ-ment (80–100 °C b T b 150–200 °C) fluctuatingmainly between 80 and130 °C (Orr, 1974; Krouse et al., 1988; Machel, 1987). Sulfur isotopecompositions of sulfides generated through BSR are around 40‰lower than those of the original sulfates (Ohmoto and Rye, 1979;Ohmoto, 1986). However, fractionation induced by TSR can producesulfides with δ34S values around 15‰ lighter than those of the parentsulfates (Orr, 1974). If sulfide precipitation follows sulfate reduction,the difference between the δ34SSO4

and δ34SH2S is approximately 14 to24‰ (Krouse et al., 1988). For Bou Dahar, the difference Δsulfate–sulfide

(δ34Ssulfate − δ34Ssulfide) fluctuates from 8.6‰ to 24.4‰. These valuesare within the range of 14 to 24‰ produced by TSR, and thus areconsistent with the reduction of sulfates through TSR. The separationΔsulfate–sulfide is generally around +5‰ for in situ-formation of H2S in ashallow environment (Ohmoto et al., 1985). This separation, however,oscillates between 0 and +10‰ for H2S generated in depth andtransported to the ore site (Ohmoto et al., 1985). It follows that the ob-servedΔsulfate–sulfide values at BouDahar indicate that the reduced sulfurwas produced in depth by TSR distant from the orebodies. Subsequent-ly, this reduced sulfur was carried toward the loci of ore deposition.

However, the overall positive δ34S values of sphalerite and galena,and the small deviation from the isotopic values of Mesozoic seawatersulfate (13–20‰, mean ~ 15‰) can also be produced by BSR in a closedsystem, or through the mixing of reduced sulfur from multiple sourcesinvolving more than one reduction process. Because the temperatureof ore deposition generally exceeded the conditions capable of sustain-ing efficient bacterial processes, biogenic sulfate reduction could haveoccurred away from the ore zone and/or prior to the hydrothermalevent.

7.4. Processes of ore deposition

The new data presented here reveal that the carbonate-hosted BouDahar Zn–Pb–Ba ores have many geological and geochemical featuresthat are typical of MVT lead–zinc ore deposits (e.g., Sverjensky, 1986;Leach et al., 2005). There are three historically proposedmodels that ac-count for the precipitation of MVT ore deposits: the reduced-sulfurmodel, the sulfate-reduction model, and the mixing model.

In the sulfate reduction model, ore metals and sulfates aretransported together. The precipitation of ore occurs during the reduc-tion of sulfate via thermochemical sulfate reduction and/or bacterialsulfate reduction in the presence of organic matter or methane(Anderson, 1983; Macqueen and Powel, 1983).

In the reduced sulfur model, ore metals and the reduced sulfur aretransported in the same fluid. The amounts of metals and sulfurtransported are very limited due to the constraint on the solubility ofmetals in the presence of sulfur. The precipitation of the ore occursdue to the PH change, cooling, and/or dilution by a superficial fluid(Anderson, 1973; Helgeson, 1970; Sverjensky, 1981).

In the mixing model, ore metals are transported by one fluid whilesulfur is separately transported by another fluid. The precipitation oc-curs as a result of themixing of these two fluids at the site of deposition(Anderson, 1973; Beales and Jackson, 1966; Anderson and Macqueen,1988; Sverjensky, 1986; Plumlee et al., 1994). Another variant of thismodel is the possibility of a metal-bearing fluid encountering a reducedsulfur source such as H2S reservoir gas, diagenetic iron sulfides, or sulfurassociated with organic matter (Beales and Jackson, 1966; Sverjensky,1986).

For the BouDahar district, transport ofmetals togetherwith reducedsulfur (reduced sulfur model) in a carbonate environment (Liassiccarbonate aquifer) is highly unlikely. In fact, the transport of reducedsulfur requires acidic conditions, which are difficult to maintain in aLiassic carbonate aquifer through which fluids have migrated overlarge distances.

Similarly, the metal-bearing fluid, migrating upward, cannot carrysulfates (sulfate reduction model) because of the low solubility of Baand Sr in an SO4

2−-rich fluid. It follows that the plausible transport sce-nario is that deep-seated fluids carriedmetals, while SO4

2−was suppliedby another shallower and cooler fluid (mixing model). The reducedsulfur must, then, have been generated via TSR of dissolved seawatersulfate (SO4

2−), and delivered to the site of ore deposition where itwas mixed with the ore-bearing hot fluid causing the precipitation ofthe ore.

The trend δ34SPbS N δ34SZnS is observed for all ore deposits exceptToutia and CorneWast, which suggests that ore precipitated under dis-equilibrium conditions that are typical of ore formation at temperatureswell below 250 °C (Ohmoto and Rye, 1979; Ohmoto, 1986). For CorneWast and Toutia, the sulfur isotopic composition trend (PbS b ZnS)may indicate equilibrium conditions. The fractionation factors betweensphalerite–galena pairs in CorneWast and Toutia have an average valueof 2.3‰ and 4.7‰, respectively. Using the equation α ZnS–PbS =(0.73/T2) × 106 (T in Kelvin) (Ohmoto and Rye, 1979), the calculated av-erage temperatures are about 290 °C and 121 °C for Corne Wast andToutia, respectively. The calculated temperature for Toutia (121 °C) iswithin the range of those reached through the fluid-inclusion studies(Th=142–180 °C). Thismay suggest that the precipitation of sphaleriteand galena took place at/or near equilibrium conditions in this deposit.However, the calculated temperature for CorneWast (290 °C) is higherthan the homogenization temperature range of 106–180 °C, obtainedfrom the fluid inclusions. This observation together with the generaltrend δ34SPbS N δ34SZnS indicate that the ores were, overall, precipitatedunder disequilibrium conditions resulting from fluid mixing (Ohmoto,1986). At the hand specimen scale, the enrichment trend of δ34S alongthe paragenetic sequence ZnS b PbS b BaSO4 is observed. This isotopiccomposition trend indicates that δ34S of the generated H2S is lighter inthe beginning, and becomes progressively heavier with time. This isconsistent with heavy δ34S and δ18O measured in sulfates (barite andcelestite). It follows that these sulfate minerals precipitated from a34S- and 18O-enriched sulfate reservoir.

The proposed fluid mixing mechanism is supported by fluid inclu-sions and stable isotope results. In fact, the similarity between theδ13C values of gangue carbonates and those of the host rocks points tothe mixing of metal-bearing and reduced sulfur-bearing fluids at thesite of deposition. A similar conclusion was reached for Polaris ore de-posits, Canada (Savard et al., 2000). The pre-ore wall–rock silicificationindicates that hot fluids underwent conductive cooling as they encoun-tered carbonate host rocks (Fournier, 1985) prior to this fluid mixingprocess.

In the early hydrothermal stage, the mixing of the deep-seated, as-cending, ore-forming, 18O-enriched hot brines with a shallow, cooler,less saline, H2S-rich fluid (trend 1) (Fig. 13) occurred at the site ofdeposition. H2S was generated through TSR processes at elevated

1084 L. Rddad, S. Bouhlel / Ore Geology Reviews 72 (2016) 1072–1087

temperatures away from the ore site. Suchmixing accounts for thewiderange of salinity and the homogenization temperatures obtained fromsphalerite-hosted fluid inclusions. During this mineralization event,the brine/shallow-fluid mixing ratio was high and resulted in hot(~143 °C) and saline (~23wt.% NaCl eq.) brine fromwhich sulfides pre-cipitated. The metal-bearing fluid was supersaturated in iron, andmixing led to the rapid precipitation of pyrite as indicated by itscolloform texture (Roedder, 1968) (e.g., Yacoub). The medium- tocoarse-grained texture of sphalerite and galena, observed in the studiedore deposits, suggests a relatively slow precipitation of sphalerite andgalena from a relatively less saturated fluid. With time, the mixing pro-portion of the brine relative to superficial fluid decreased as the cool su-perficial SO4

2−-rich fluid started to dominate the hydrothermal system.This is evident from the overall cooling trend (Trend 2) (Fig. 12). Atthis waning stage, the SO4

2− could not be reduced most likely becauseof lower temperatures that hindered the TSR processes, and thus theproduction of H2S (Kiyosu and Krouse, 1990; Machel et al., 1995). Theinhibition of TSR reaction contributed to the end of the sulfide mineral-izing stage. The unreduced SO4

2− combined with Ba leading to the pre-cipitation of barite from a cooler (Th b 50 °C, ~40 °C) and moderatelysaline fluid (~17 wt.% NaCl eq.). The precipitation of barite was slowas revealed by its coarse-grained texture. At the final waning stage ofthe evolution of the hydrothermal fluid system, the cooler fluid becamedominant and more pronounced giving rise to a cooler (Th b 50 °C, ~40 °C) and diluted fluid (~5 wt.% NaCl eq.). As a result of this cooling-dilution process, Sr combined with the unreduced SO4

2− causing theslow precipitation of celestite (Trend 2) (Fig. 13). The presence ofiron-oxide inclusions in celestite reflects the oxidative nature of thefluid system during the last waning stage.

7.5. Ore controls, timing of mineralization, and fluid migration

Lithostratigraphy, faults, and local paleostructures have guided theore emplacement in the Bou Dahar district. The E–W- to NE–SW-trending faults at the margins and across the Bou Dahar plateau(Fig. 1) were a major control for ore deposition. Faulting activities dur-ing the first Liassic rifting had created a paleohigh structure, adjacent todeep basins, which promoted the development of the Lower andMiddleLiassic carbonate platforms. It is within these highly porous carbonatesthat the strata bound-type and the vein-type ore deposits are confined.During the second Liassic–Jurassic rifting, the Liassic carbonates weredrowned and sealed with the Toarcian–Bajocian impermeable marls.The latter acted as an aquitard focalizing the mineralizing fluids withinthe Liassic carbonates. Later on, these faults and fractures werereactivated during the Alpine orogeny and acted as migration conduitsfor the ascending metal-carrying fluids. Beside these structural andlithological controls, brecciation, dolomitization, and silicification hadalso enhanced porosity for ore emplacement.

The age of ore emplacement at Bou Dahar cannot be determinedprecisely. Ore deposition, however,must have takenplace after the frac-turing and faulting of the Jurassic platform. These faulting activities arerelated to Eocene–Miocene Alpine orogeny. The ore deposits aremainlyhosted in Middle Liassic carbonates. In some ore deposits, however, theore is hosted in Aalenian black shale/mudstones filling the fractureswithin the Liassic limestone. Therefore, the ore is post-Aalenian (post-Early Dogger), and thus post-Jurassic rifting. In the Tirrhist Pb–Zn oredeposit, the genesis of the mineralization is post-Jurassic (Caïa, 1968).In the EasternHigh Atlas, Pb–Zn ore deposits are hosted in rocks rangingin age from Liassic to Lower Cenomanian (Rajlich et al., 1983). It iswidely accepted that ore deposition in the High Atlas region was post-Cretaceous (Agard and Du Dresnay, 1965; Bazin, 1968; Le Blanc, 1968;Dupuy, 1984; Rddad, 1998). Moreover, the ore was emplaced prior tothe onset of the supergene oxidation of the sulfides, which took placein the last 20 Ma (Choulet et al., 2014).

There is an increasing agreement thatmajor sediment-hosted Zn–Pbores are formed as a result of large-scale tectonic triggers (Leach et al.,

2010) that released deep-seated fluids into favorable geochemicaltraps. This is themost plausible mechanism behind large-scale fluid cir-culation in the Bou Dahar district and other ore deposits of the HighAtlas foreland belt. A post-Cretaceous compressional tectonic event(Alpine orogeny) took place during the collision between theEuropean and African plates. The Atlasic compressional tectonic eventwas not continuous, but rather consisted of a succession of periods ofshortening alternating with periods of tectonic quiescent (Frizon deLamotte et al., 2009). Consequently, the timing of ore deposition inthe studied area can be related to the first major Atlasic compressionalevent which started during the Middle–Eocene age (~50 Ma–35 Ma)and continued during the second compressional event of the Late Mio-cene (Tortonian) age (~12 Ma). This age range is consistent with theones proposed for the Touissit–Bou Beker ore district (Bouabdellahet al., 2012) and for the Tunisian Pb–Zn ore districts (Bouhlel et al.,2013).

This major tectonic event has caused N–S trending compression ofthe High Atlas, which resulted in creating a topographic gradient.Compression and topography-driven processes are found to be effectivemechanisms in remobilizing and transporting large amounts of orogen-ic, metal-rich brines from the basin to adjacent platforms (Garven andFreeze, 1984; Garven, 1985; Kesler, 1994). This mechanism is wellestablished in the genesis of the Pb–Zn–Ba MVT in the Ozark Plateauin USA (Leach, 1994; Appold and Garven, 1999; Leach et al., 2005;Leach et al., 2010). Thrusting, regional E–W and NE–SW deep-seatedfaults acted as pathways for the flow andmigration of fluids. The Alpineorogeny as a driving force for the circulation of large-scale fluids wasalso proposed for the Pb–Zn–Ba MVT ores in the Tunisian Atlasic belt(Bouhlel, 2005) and for theMVT Pb–Zn–Ba-(±Sr) ores in theMoroccanHigh Atlas (Rddad, 1998; Rddad, 2012).

The proposed mechanism of the orogenically-driven circulation ofbrines in crustal rocks, followed by the ascent of and reactionwith fluidsin the overlaying cover rocks has striking similarities to themechanismsthrough which other MVT deposits formed as a consequence of theplate tectonic collisions (Bradley and Leach, 2003).

8. The Bou Dahar ore genesis model

Based on the geochemical studies, in combination with geologicaland mineralogical characteristics, salient physico-chemical metallogenicparameters can be drawn for the Bou Dahar ore genesis. These parame-ters include temperature and salinity during ore formation, the charac-ter and source of hydrothermal fluids, and the sources of sulfur andmetals. These constraints are used to establish the following geneticmodel for the origin of the Bou Dahar ore deposits.

The Eocene–Miocene Alpine orogeny caused the compression of theHigh Atlas basin, via a thick-skinmodel (Teixell et al., 2003), and the de-velopment of a topographic gradient. The deep-seated, ore-formingfluids were expelled during sediment compaction (Noble, 1963;Beales and Jackson, 1966) and subsequently remobilized to higher plat-form zones (e.g., Bou Dahar paleohigh) by the Alpine tectonic orogenyand topographic gradient (e.g., Garven and Freeze, 1984). These basinalfluids are brines as indicated by microthermometric and stable isotopecharacteristics. The ore-forming brines, driven by the Alpine tectonicorogeny, acquired their high salinity mainly from evaporated seawatertrapped in sediments, with aminor contribution fromhalite dissolution.During their migration, the bittern brines evolved to Pb–Zn–Ba-richfluids through the interaction with the Paleozoic and the Mesozoicsiliclastic rocks. The overpressured, orogenic, metal-rich fluids were,subsequently, channeled through the inherited deep-seated E–W toNE–SW faulted zones. Ultimately, they migrated through the confinedLiassic carbonate reservoir that contained H2S-rich fluid generatedthrough TSR processes away from the ore site. The mixing of thesetwo fluids triggered the precipitation of the sulfide ores. During thelate stage, the hydrothermal system was open to continual influx ofSO4

2− rich fluids, resulting in an increase in the proportion of the SO42−

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rich, cooler fluid relative to the brine. At this waning stage, barium andstrontium reacted with SO4

2− leading to the precipitation of barite andcelestite respectively.

The BouDahar ore district exhibits striking similarities to the Centraland SoutheastMissouriMVTdistricts in terms of its fluid characteristics.In these districts, the sphalerite-hosted fluid inclusions indicate homog-enization temperature in the range of 80 to 110 °C, and a salinity ofmore than 22wt.%NaCl eq. (Leach, 1980). Because of the contrasting sa-linity and temperature values in thefluids forming sphalerite and barite,Leach (1980) argued that the precipitation of barite is unrelated to andsuperimposed on sulfide mineralization. For the Bou Dahar district, al-though sulfides and sulfates show distinct fluid temperatures, they re-flect an overlap in salinity values. Therefore, the sulfide and sulfatehydrothermal stages were likely related, and were formed from thesame evolving hydrothermal brine. The proposed ore genesis model,which involves the interaction between basement-derived ore fluidsand shallower H2S-rich fluids, bears similarities to numerous MVT oredeposits worldwide (e.g., Ozarks, USA, Leach, 1994; Pine Point Canada,Rhodes et al., 1984).

9. Concluding remarks

Geological, mineralogical, fluid-inclusion, and C–O–S–Pb isotopestudies allow a better understanding of the genesis of the Bou DaharPb–Zn–Ba-(±Sr) ore district. The following are insights into the genesisof the mineralization:

1. The carbonate reservoir developed during the Liassic period and frac-tured during the Eocene–Late Miocene orogeny. It was sealed withthick, mainly marls and argillaceous limestone of Middle and LateJurassic. The carbonate reservoir provided circulation pathways anda favorable site of ore depositionwhile the overlappingmarls provid-ed a trap for fluid circulation.

2. The sulfur needed for the precipitation of the sulfide ore depositswasgenerated through TSR of dissolved Mesozoic sulfate away from thesite of mineralization. Ultimately, the sulfur was delivered to theloci of ore deposition.

3. The bittern fluids evolved to Pb–Zn–Ba-rich fluids through the inter-action with the Paleozoic siliciclastic basement and the Mesozoiccover. The post-Cretaceous Alpine orogeny triggered the remobiliza-tion and circulation of these metal-carrying fluids along E–W toNE–SW faulted zones toward the site of deposition.

4. At the site of ore precipitation, the ore-forming fluids mixed andreacted with a subsurface cooler H2S-rich fluid to form sulfides. Dur-ing the waning hydrothermal stage, the excess of unreduced sulfurand the continual influx of dissolved sulfate reacted with bariumand strontium to form barite and celestite.

The geological, mineralogical, and geochemical characteristics of theBou Dahar mining district allow its integration into the large class ofMississippi-Valley-Type ore deposit. The Bou Dahar characteristics areconsistent with those of other Pb–ZnMVT districts and provinces docu-mented in others regions in the world (e.g., Ozarks, USA, Leach, 1994;Appalachian, USA, Kesler, 1996; Pine Point Canada, Rhodes et al.,1984; High Atlas, Rddad, 1998; Reocin, Spain, Velasco et al., 2003;Touissit–Bou Beker district; Moroccan–Algerian confines, Bouabdellahet al., 2012; and Tunisia Alpine Pb–Zn districts, Bouhlel, 2005).

Acknowledgments

The authors would like to thank the Professional Congress Staff/CityUniversity of New York for the grant that financially supported the C–O–S–Pb isotope analyses. We would also like to thank Prof. Bouabdellah,Mohammed and Prof. Canals, Àngels whose constructive comments onthe first draft have greatly improved the quality of this paper. We arealso grateful to Prof. Albarède, Francis for his constructive comments onthefirst draft, and for Pb isotope analyses at the EcoleNormale Supérieure

in Lyon, France. Wewould also like to acknowledge the thorough reviewand constructive comments of an anonymous reviewer. We would likealso to express our gratitude to Franco Pirajno for his comments and forhandling our manuscript.

Appendix A. Supplementary data

Supplementary data associated with this article can be found in theonline version at http://dx.doi.org/10.1016/j.oregeorev.2015.08.011.These data include the Google map of the most important areasdescribed in this article.

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The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

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The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

Ore Geology Reviews

Volume 72, Part 1, January 2016, Pages 1072–1087

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

Larbi Rddada, , ,Salah Bouhlelb

Show moreShow less

Highlights

•

The carbonate reservoir developed during the Liassic period and fractured during the Eocene–Late Miocene orogeny. It was sealed with thick, mainly marls and argillaceous limestone of Middle and Late Jurassic.

•

The sulfur needed for the precipitation of the sulfide ore deposits was generated through TSR of dissolved Mesozoic sulfate away from the site of mineralization.

•

The post-Cretaceous Alpine orogeny triggered the remobilization and circulation of these metal-carrying fluids along E–W to NE–SW faulted zones toward the site of deposition.

•

At the site of deposition, the ore-forming fluids reacted with a subsurface cooler H2S-rich fluid to form sulfides. During the waning hydrothermal stage, the excess of unreduced sulfur reacted with barium and strontium to form barite and celestite.

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

Abstract

The Bou Dahar Pb–Zn–Ba (± Sr) is hosted in the Lower and Middle Liassic carbonate platform in the oriental High Atlas of Morocco. The paragenetic sequence includes quartz–pyrite–melnicovite–sphalerite–galena–calcite–barite ± fluorite– ± celestite. Fluid-inclusion studies were conducted on sphalerite (early mineralizing stage) and barite, and celestite (late mineralizing stage). These studies reveal two end-member fluids, a hot (~ 143 °C) and saline fluid (~ 23 wt.% NaCl eq.) and a cooler (< 50 °C) and diluted fluid (~ 5 wt.% NaCl eq.). Based on fluid-inclusion and C–O–S isotope studies, a conclusion is reached that the Bou Dahar ore deposits were formed by the mixing of two fluid — a diluted, SO2 −

4-rich fluid, and an 18O-enriched basinal brine that carried Pb, Zn, and Ba. The sulfur required for the precipitation of sulfides was generated by the thermochemical sulfate reduction of dissolved sulfate (SO4

2 −) of the Mesozoic seawaters, and delivered to the site of ore deposition. The sulfur of sulfate minerals was derived directly from these dissolved SO4

2. The Pb isotope compositions are homogenous with 206Pb/204Pb, 207Pb/204Pb, and 208Pb/204Pb ratios ranging from 18.124 to 18.183, 15.630 to 15.634, and 38.325 to 38.440 respectively. This Pb isotope composition is indicative of an upper crust and orogene reservoirs as the source of lead and other metals. The emplacement of mineralization occurred during the Eocene–Miocene Alpine orogeny, and tectonic burial and compression were the driving forces behind the circulation of the orogenic-brines. These ore-forming fluids migrated, along thrusting regional E–W and NE–SW deep-seated faults, to the confined carbonate-Liassic reservoir.

Keywords

MVT Pb–Zn–Ba;Fluid inclusions;C–O–S–Pb isotopes;Oriental High Atlas;Morocco

Corresponding author.

Published by Elsevier B.V.

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The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

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http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

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The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

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The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

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The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

The Bou Dahar Jurassic carbonate-hosted Pb–Zn–Ba deposits (Oriental High Atlas, Morocco): Fluid-inclusion and C–O–S–Pb isotope studies

http://www.sciencedirect.com/science/article/pii/S016913681530010X[12/01/2016 13:41:13]

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