The Jbel Saghro Au(–Ag, Cu) and Ag–Hg Metallogenetic Province: Product of a Long-Lived Ediacaran Tectono-Magmatic Evolution in the Moroccan Anti-Atlas
Abstract
:1. Introduction
2. Geological Overview of the Anti-Atlas Mountains
3. Tectono-Magmatic Evolution of the Jbel Saghro
3.1. The Lower Complex and the D1 Transpressive Tectonics
3.1.1. The Earlier Arc-Related Metagreywackes and Metavolcanic Rocks
3.1.2. The Intrusive Rocks
3.1.3. The Main Pan-African D1 Deformation Event
3.2. The Upper Complex or the Inception of a Silicic Large Igneous Province
3.2.1. Generalities
3.2.2. The Qal’at Mgouna Ash-Flow Caldera
- (i).
- A lowermost pyroclastic layer consists of a 400–500 m thick, unwelded to slightly welded, moderately crystal-rich dacitic lapilli tuff (Figure 6c,d and Figure 7a,b) interpreted as an ash-flow deposit [142,143]. Internal stratification of the ash-flow tuff is crude, oriented N060–080°E 80°NW, as highlighted by discrete layers which are either pumice-richer, lithic-richer or entirely devitrified with spherulites. In a specific layer 40 m thick, greenish fibrous pumices displaying silicified tubular micro-vesicles and a silky/fibrous fabric can reach up to 5 cm long. Lithic clasts up to 20 cm in size are common throughout and consist mainly of basement greywackes, lavas and quartz-rich ignimbrite fragments. Phenocrysts are mostly broken plagioclase and K-feldspar, in various ratios with minor amounts of chloritised ferro-magnesian crystals (biotite and probable amphibole) and very scarce quartz.
- (ii).
- Above the ash-flow unit lies a ca. 200 m thick volcano-sedimentary (epiclastic) unit with very thin bedding (Figure 6d and Figure 7a,b). The lower part (100 m thick) is made of layered tuffaceous breccias containing ignimbrites fragments. The upper part consists of laminated reddish and greenish mudstones and sandstone oriented N070°E 70°NW. When preserved from important silicification, the identifiable components are microscopic broken crystals and lithic fragments. Beds are broadly continuous laterally, being only sometimes disrupted by syn-sedimentary normal faults and slump-like structures. Faults are roughly oriented NW–SE. Fluid escape textures are common and allow assessment of the polarity of the intra-caldera sequence. All sedimentological features argue for a subaqueous emplacement, at least for the upper part of the epiclastic unit. In our model, and as no marine sediments have been hitherto recognised in the entire Jbel Saghro in the Ediacaran formations, such subaqueous environment may be reasonably related to a caldera lake.
- (iii).
- Above the volcano-sedimentary unit lies a ca. 200–300 m thick crystal-rich rhyolitic ash- and-lapilli tuff (Figure 6d and Figure 7a–c). Plastic deformation due to significant compaction is evidenced by reddish flattened pumices (Figure 6e). Glass shards and broken phenocrysts are visible under the microscope (Figure 6f). Phenocrysts are quartz, plagioclase, K-feldspar, and scarce amounts of chloritised Fe–Mg minerals (biotite and amphibole). Up to 2 m-sized lithic clasts are abundant, especially in the basal part, and consist of metagreywacke, ash-flow tuff fragments, jasperoids and monzogranite (Figure 6e). This voluminous quartz- and pumice-rich unit is readily interpreted here as a welded ignimbrite.
- (iv).
- The top of the sequence is dominated by massive andesite lava flows and epiclastic polylithologic breccias (Figure 5, Figure 6d and Figure 7a,b). The bottom of this whole sequence is intruded by a monzogranite porphyry (Figure 5 and Figure 7a,b). Plugs of similar porphyry facies also locally intrude the upper parts of the sequence. Such porphyry is here interpreted as a resurgent pluton [137,144] that tilted the intra-caldera sequence upon emplacement [47]. Because of the tilting, the thickness of the intra-caldera sequence is exposed over 1500–2000 m, of which 800–1000 m consists of ash-flow tuffs and epiclastic rocks. To the north, the intra-caldera sequence disappears beneath the young sedimentary rocks of the Dadès valley (Figure 5).
3.2.3. The D2 Deformation Event
4. Characteristics of Ore Deposits
4.1. The Thaghassa Intrusion-Related Gold Deposit
4.2. The Qal’at Mgouna Au–Ag (Cu, Mo, Bi, Te) District
4.2.1. The Isamlal Porphyry Au(–Cu–Mo) Deposit
4.2.2. The Qal’at Mgouna Au–Ag(–Bi–Te) Epithermal System
4.3. The Zone des Dykes Intermediate Sulfidation Epithermal Au-Base Metal Deposit
4.4. The Giant Ag–Hg Imiter Deposit
5. Discussion
5.1. A Simplified Tectono-Magmatic Evolution Model of the Eastern Anti-Atlas
5.1.1. The Lower Complex and the D1 Deformation
5.1.2. The Upper Complex and the D2 Deformation
5.1.3. About the Transition between the Two Complexes and the D1 and D2 Tectonics
5.2. The Mineralising Model
- The first stage shows strong magmatic influence. It is characterised by emplacement of porphyry stocks, aplite dykes and sills at high temperatures from 400 °C up to 600 °C. At Thaghassa, this stage was responsible for the partial melting of the metagreywackes in response to the Ikniwn granodiorite thermal effect and for the related genesis of leucocratic S-type haplogranitic sills. In the Qal’at Mgouna district, this stage was responsible for the formation of stockscheider and miarolitic cavities within sills and dykes.
- The second intermediate stage consists of magmatic-hydrothermal vein emplacement and associated pervasive alteration. The persistence of the magmatic character is shown by the occurrence of high-temperature alteration phases such as tourmaline, micas, andalusite, apatite, K-feldspar with quartz. In the Qal’at Mgouna district, at Isamlal, this stage can be compared with the classical potassic and magnetite alteration in some porphyry type systems [190]. It is also marked by the wide pervasive development of Al-silicate–Al-hydroxide–phosphate–muscovite–F-rich phlogopite and F-rich tourmaline alteration, related to the late Si-rich alkali granites. K-feldspar, apatite, white mica along vein rims are observed at the beginning of vein aperture at Thaghassa. Temperatures of formation are bracketed between 250 and 500 °C.
- The third stage is hydrothermal and formed at lower temperature (60 < T (°C) < 300) producing gangue minerals except for the Thaghassa and Isamlal deposits where high-temperature minerals were also formed (350–450 °C). This stage end with the emplacement of economic ore.
5.3. Implication of the Tectonic Regime Changes for the Late Neoproterozoic—Early Cambrian Geodynamic Evolution and Ore Deposit Emplacement
6. Conclusions
Author Contributions
Funding
Acknowledgments
Conflicts of Interest
References
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The Zone des Dykes Deposit | The Qal’at MGouna District | The Thaghassa Deposit | The Imiter Deposit | ||
---|---|---|---|---|---|
Stage I (strong magmatic affinities) | Not expressed | Granodiorite stock emplacement and fluid exsolution | Alkali-granite emplacement with quartz, K-feldspar, F-tourmaline, F-muscovite in miarolitic cavities and stockscheider (400 < T °C < 600) 1 | Aplite dyke emplacement (500 < T °C < 600 °C) 1 | Not expressed |
Stage II (intermediate stage between magmatic and hydrothermal conditions) | Not expressed | K-feldspar and magnetite alteration (disseminated and in veinlet stockwork) | Strong alteration with quartz, F-tourmaline, F-Cl-micas, andalusite, F-Cl apatite, monazite (250 < T °C < 400) 1 | Quartz, K-feldspar, muscovite, apatite, tourmaline and apatite (T °C < 500) 1 | Not expressed |
Stage III (hydrothermal) | Quartz, adularia veins with calcite, chlorite, sulfides and gold (210 < T °C < 280) 1 | Quartz stockwork with Cl-biotite, Cl-amphibole, muscovite, sulfides (Cu–Mo) and gold (160 < T °C < 460) 1 | Chlorite-rich breccias, thenAdularia, specularite, quartz veins with sulfides and ″gold″ (160 < T °C< 200) 1 | Striped quartz veins filled by quartz, sericite, sulfides and gold (300 < T °C < 450) 1 | Firstly, quartz-adularia veins with silver-rich sulfides and alloys (100 < T °C < 280) 1 and then dolomite-quartz veins with Ag-rich galena and sphalerite (60 < T °C < 110) 1 |
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Tuduri, J.; Chauvet, A.; Barbanson, L.; Bourdier, J.-L.; Labriki, M.; Ennaciri, A.; Badra, L.; Dubois, M.; Ennaciri-Leloix, C.; Sizaret, S.; et al. The Jbel Saghro Au(–Ag, Cu) and Ag–Hg Metallogenetic Province: Product of a Long-Lived Ediacaran Tectono-Magmatic Evolution in the Moroccan Anti-Atlas. Minerals 2018, 8, 592. https://doi.org/10.3390/min8120592
Tuduri J, Chauvet A, Barbanson L, Bourdier J-L, Labriki M, Ennaciri A, Badra L, Dubois M, Ennaciri-Leloix C, Sizaret S, et al. The Jbel Saghro Au(–Ag, Cu) and Ag–Hg Metallogenetic Province: Product of a Long-Lived Ediacaran Tectono-Magmatic Evolution in the Moroccan Anti-Atlas. Minerals. 2018; 8(12):592. https://doi.org/10.3390/min8120592
Chicago/Turabian StyleTuduri, Johann, Alain Chauvet, Luc Barbanson, Jean-Louis Bourdier, Mohamed Labriki, Aomar Ennaciri, Lakhlifi Badra, Michel Dubois, Christelle Ennaciri-Leloix, Stanislas Sizaret, and et al. 2018. "The Jbel Saghro Au(–Ag, Cu) and Ag–Hg Metallogenetic Province: Product of a Long-Lived Ediacaran Tectono-Magmatic Evolution in the Moroccan Anti-Atlas" Minerals 8, no. 12: 592. https://doi.org/10.3390/min8120592