Revised Stratigraphy and Mineral Resources of Balochistan Basin, Pakistan: An Update

The Balochistan basin is located on the south western part of Balochistan Province and also Pakistan. Balochistan super basin is subdivided into northern Balochistan (Pishin basin or Kakar Kohorasan basin represented as back arc basin), central Balochistan (Chagai-Raskoh-Wazhdad Magmatic arc and Hamuns-Inter arc basin) and southern Balochistan (Makran Siahan basin) basins. Balochistan basin consists of Cretaceous to recent sediments, diverse igneous rocks and low grade metamorphics. Balochistan basin is a leading basin which consists of very significant mineral deposits especially copper and gold deposits. These mineral resources need to be developed for the development of areas, province and Pakistan. During previous half century a lot of geological work has been done in Balochistan basin. Here the revised stratigraphic set up and its mineral resources with an update are being presented.


Introduction
All the mineral resources (except the radioactive/nuclear minerals and petroleum) are responsibility of federating units/provinces (Balochistan, North Punjab, South Punjab, Sindh, Khyber Pakhtunkhwa), Capital Islamabad, Gilgit Baltistan and Azad Kashmir while the Radioactive minerals and Petroleum (oil and gas) are under the jurisdiction of Federal government of Pakistan. Keeping in mind this, the every province should know the potential of their mineral resources, so this paper on Balochistan Basin (along with other papers on north Punjab, South Punjab, Khyber Pakhtunkhwa/KP, Balochistan and Sindh) is ar-fossil collection source. The source of this formation is mostly Hinterland and partially Indus Suture. The tentative thickness ranges from 400 -1200 m. The lower contact with the Nisai formation and upper contact with Shagala formation seems to transitional and conformable. According to stratigraphic position, its age is supposed to be Early Eocene based on correlation with Early Eocene Shaheed Ghat shale of Sulaiman basin.
Mina Formation: It is named by [46] [12]. It consists of terrestrial sandstone and shale but at places conglomerate and limestone. The sandstone is fine to coarse grained, gritty, thin to thick bedded, grey to greenish grey, brown and weathers light grey, brown, rusty with patches of black desert varnish on its surface. In the central and eastern part of Kaker Khurasan range the sandstone is more coarsely grained and thick bedded than western part. It shows the source from the Indus Suture, however the western part may have northern and northwestern source.
Some sandstone is pebbly, red and maroon. Cross bedded and ripple marks are common. The shale is maroon, red ochre type, grey, greenish grey and calcareous. The red and maroon color is dominant in the Kaker Khurasan area while grey to greenish grey shale color is dominate in the southern Balochistan basin.
It is 3000 m thick and only exposed in the northern Balochistan Basin (Kakar-Khorasan range). This formation shows the continental (Molasse) conditions in the Kaker Khurasan range. Continental vertebrate bones of rhinoceros, crocodiles, wood fossils, etc [80] [81] [82] are also found in the Kaker Khurasan areas. Recently [80] [81] [82] found a baluchithere Pakitherium shagalai with his baby. Pakitherium shagalai-a baluchithere reported first time in Balochistan basin. Its age is middle-Late Eocene deduced from correlation with terrestrial Kingri Formation of Chamalang (=Ghazij) Group.
Vihowa Group: Vihowa group represents Chitarwata, Vihowa, Litra and Chaudhwan formations [83]. Vihowa Group is correlated with Multana formation [12] after Multana/Multanai Kili (39 E/4) west of Mina Bazar railway station. It consists of conglomerate with subordinate shale and sandstone. Its considered age is Oligocene-Pliocene. Sakhi Sarwar Group: It is first used by [43] after Sakhi Sarwar area of Dera Ghazi Khan. It is synonymous with Boston formation. It represents Dada (mainly conglomerate) and Sakhi Sarwar Formation named by [43] (mud and sandstone with poorly developed conglomerate, while in centre of valleys the mud is dominant) concealed at places especially in the valleys and plain areas by the Subrecent and Recent fluvial, eolian and colluvial deposits. Its considered age is Pleistocene to Holocene.
Makran Mud volcanoes: The Makran mud volcanoe is exposed north of Qila Saifullah just on the western side of road (Qila Saifullah-Sharan Jogezai road). The mud is being erupted so far. For detail pl. see in Makran Siahan basin.
Subrecent and Recent fluvial, eolian and colluvial deposits: These are also found in the valleys and vicity areas and along and in the stream channels.

Revised Stratigraphy of Central Balochistan Basin (Chagai-Raskoh-Wazhdad Magmatic Arc and Hamuns-Inter Arc Basin)
The Balochistan magmatic arc is located in the central Balochistan basin and consists of Chagai-Raskoh-Wazhdad magmatic arc and Hamuns-Inter arc basins. The Chagai-Raskoh magmatic arc shows Cretaceous to recent deposition ( Figure 1). The revised stratigraphy of central Balochistan basin (Figure 1) is as follows.
Sinjrani Volcanic Group: It was introduced by [12] after Sinjrani tribe of Chagai. It consists of agglomerate, volcanic conglomerate, tuff and lava with subordinate shale, sandstone and limestone. It includes Basaltic-andesitic lava flows and volcaniclastics, with minor shale, sandstone, siltstone, lenticular bodies of limestone and mudstone. It is Middle to Late Cretaceous (Aptian to Santonian). This group was invaded during Late Cretaceous to Pleistocene by Chagai intrusions, represented by several phases including granite, adamellite, granodiorite, tonalite, diorite and gabbro. Its thickness is 900 -1200 m. Kuchaki Volcanic Group (equivalent of Sinjrani Volcanic Group) is named for the village of Kuchaki (34 G/8) about 63 km southwest of Ahmad Wal [12]. It consists of volcanic agglomerate, lava, tuff, with subordinate inpersistent limestone, tuffaceous shale and sandstone near the top of the assemblage. The upper contact with Humai Formation is generally conformable and lower contact is not exposed. Its age is Late Cretaceous.
Chagai Intrusions: It includes quartz hornblende diorite, normal diorite and biotite granite. Micropegmatitic quartz diorite is reported from Koh Naro. It is large batholiths that are invaded in Sinjrani volcanic group. The age is Late Cretaceous and later [12].
Humai Rakhshani Formation: Humai and Rakhshani formations were introduced by [12] from Koh Humai (hill of Kohi Sultan) in the eruptive zone and Rakhshani belt on eastern end of Dalbandin valley respectively for the mixed lithology which included the "Hippuritic limestone" of [84]. Conglomerate at the base, intercalations of shale, sandstone, siltstone and limestone in the middle and thick bedded to massive limestone at the top are reported. The formation overlies unconformably the Chagai Intrusion/Sinjrani Volcanic Group along the southern margin of the Chagai hills but in other areas has also a disconfirmable contact through the presence of basal conglomerate. It is correlated with Akhtar Nika Formation of Sharan Jogezai Group. It also includes the Juzzak Formation, lower half of Gidar Dhor Group and basal part of Pishi Group of [12]. It consists of intercalations of sandstone, shale, mudstone and limestone representing turbidite sequence, andesitic lava flows and volcaniclastics. Its age is Late Cretaceous to Early Paleocene. It is correlated wit Jabrai Formation of Sharan Jogezai Group. The age is Late Cretaceous (Campanion-Maastrichtian) [12].
Bunap Opiolite Complex: It includes the obducted ophiolite mélange which includes gabbro, diorite and serpentinite. The basic type contains pyroxene and amphibole. Its age is Latest Cretaceous or Paleocene.
Kharan Limestone: It is named by [12] after Kharan valley. It consists of medium to thick bedded foraminiferal and argillaceous limestone. Tanki sills consisting of mainly pyroxene diorite are located in the Robat limestone. Its age seems to be Paleocene. Kharan Limestone is considered as synonym with the Nisai Group (Robat and Nisai formations).
Saindak Formation; The name is derived from Saindak Fort (a large syncline) which has been designated as the type locality [12]. Its synonyms are Washap formation at Gwalishtap near the Pakistan-Iran boarder and the Amalaf formation. It consists of shale, siltstone, sandstone, marl and limestone with andesitic lava flows and volcaniclastics in the lower part. It is Early to Late Eocene. It is correlated wit Murgha Faqirzai shale of Shagala Group in northern Balochistan and Siahan shale of Siahan group in southern Balochistan.
Shorkoh Intrusions: These are dykes or sills but a few small lenticular stocks have been found in the region of Robat and Saindak. These are hypabyssal and intermediate composition. The rocks are mainly diorite. The age is Late Eocene or later [12].
Pishi Formation (=Dalbandin Formation): Pishi Formation is named here after the Pishi group which is named after the Pishi Rud lies in the Ras Koh Range while Dalbandin Formation is named after Dalbandin valley but here not well exposed. This is the reason the name Pishi Formation is preffered. These rocks are found in between Gaukoh Hamun (30 P/15) and Bunap (34 H/5). The rocks of the group are thought to be also present in the Dalbandin synclinorium named as Dalbandin Formation [12]. It consists of shale, mudstone, soft sandstone and conglomerate. The clay is white, green, ochre and brown. The succession of dominat shale unit resembles to Hoshab shale and sandstone and shale is similar to Panjgur formation of southern Balochistan. This formation is also similar to Mina and Nauroz formations. The sandstone of the Pishi area is more gritty and thick than Dalbandin and Makran flysh indicating close to source. Its age is Oligocene to Miocene.
Kamerod Formation: It is derived from Kamerod on the northern margin of the Siahan range (31 M/10) [12]. The lithology and description is same as Kech Formation. Its age considered is Pleistocene.
Subrecent and Recent deposits: These deposits are represented by unconsolidated gravel, sand, silt and clay, and Eolian sands in the Chagai-Dalbandin trough.
Revised Stratigraphy of Wazhdad Magmatic Arc The Wazhdad magmatic arc is a northernmost part of Siahan Range and located just south of Hamun Mashkel. This is the reason its stratigraphy is reported under the southern Balochistan Basin (Figure 1). Its southern boarder with Siahan-Makran basin is being marked at the thrusted ophiolitic line on the southern base or foot of Toe Koh (just west of Washuk town; 35 A/10) ( Stratigraphy of Hamuns (inter arc) basins Hamuns basins are Inter arc basins found in the central Balochistan Basin which represents exposed eolian sand dunes covering the fluvial Pleistocene Kamerod formation (conglomerate, sandstone and clays). The older rocks may be like Chagai-Raskoh magmatic arc and Wazhdad magmatic arc.

Revised Stratigraphy of Southern Balochistan (Makran Siahan) Basin
Recently many workers carried the geological investigation in Malkan and Siahan ranges of southern Balochistan [85]- [97] and other areas. The revised stratigraphy of southern Balochistan basin ( Figure 1) including the Wazhdad magmatic arc are shown as below. Sharan Jogezai Group: The Cretaceous Sharan Jogezai Group consists of Akhtar Nika and Jabrai formations representing Parh like porcellaneous limestone, marl and shale. It is exposed near Mand [12] which is located near the Iran-Pakistan boarder.
Nisai Group: The Paleocene Nisai Group consists of Ispikan conglomerate and Wakai limestone and shale. It is exposed as lense shaped distributed as rare exposures.
Ispikan conglomerate: It is named after the village of Ispikan about 12 miles northeast of Mand (31 J/4; [12]). Conglomerate consists of pebbles of quartz, granite, andesite, and other igneous rocks. Matrix of conglomerate is chloritic (green). Its lower contact with the thin bedded marl assigned to Parh series seems to be unconformable. Its upper contact is not clear but some remnants of Wakai limestone are found at the eastern end of the hill near Ispikan which show contact with Wakai formation. Age of Ispikan conglomerate is Paleocene determined by stratigraphic position between the Cretaceous and Eocene rocks and some diagnostic fossils [12].
Wakai Limestone: It is named after Koh-i-Wakai in the valley of Tagrana Kaur (31 J/11; [12]). It consists of limestone, marl and shale. The age of formation is interpreted as Paleocene. Its synonym is Nisai Limestone. The formation is important for petroleum prospecting and source, if it has large subsurface thickness, extension and suitable conditions. Siahan Group: It is named by the [14]. It represents Siahan slates and shales, Wazhdad volcaniclastics, Washuk ophiolite complex and Washuk Intrusion.
Siahan Formation: It is named after the Siahan Ranges (31 M/8; [12]). It comprises slates and shale with siltstone, sandstone and quartzite. The lower contact is with Wakai limestone and the upper contact is with the Wazhdad volcaniclastic group which is conformable. According to [12] megafossils are rare in the shale and can not be thoroughly tested for microforaminifers, however some thin limestone beds yielded fossils which show Eocene age. According to [12] and stratigraphic position the age is Early Eocene.
Wazhdad Volcaniclastic Group: It is named after the Wazhdad Mountain (35 A/6) by [96] for Wazhdad volcaniclastic group. This is synonym and coeaval to Zurati Formation. Zurati formation is named after the Zurati Koh and Tank e Zurati 31 M/11 [92]. The Wazhdad Range is located just west of Washuk and east of Palantak. These rocks are exposed in the Wazhdad Mountain (35 A/6) and may be extending upto Toe Koh 35 A/10 ( Figure 2) in the east and Zurati Tank 31 M/11 in the west ( Figure 2). It consists of tuff, agglomerate, tuff breccias, tuffaceous sandstone and shale. These rocks are dark green colour and weather in to dark grey to black colour, hard and resistant, forming high peaks.
The estimated thickness of this formation is 1200 to 1500 m in the Wazhdad Range, the actual measurement is also difficult due to intense faultings and foldings. Their lower contact with the Siahan shale and upper contact with Hoshab shale seems to be transitional. According to law of superposition the age of Wazhdad volcaniclastic group may be early to Late Eocene.
Washuk Ophiolite Complex: It is named by the [96]. This ophiolite (part of complete sequence) is exposed in the thrusted plane of Wazhdad mountain range. The thrust line is located on the southern side of Wazhdad mountain range at Mazargati (35 A/6), Jhal Kaur (35 A/7), and Toekoh (35 A/10) and also in Zurati (31 M/11) areas ( Figure 2). The observed rocks are granite, peridotite, bronze dunite, asbestos, (serpentine), soapstone (talc), and chromite. Its exposures are small, however in the southern vicinity, there is a wide alluvium cover which may yield more ophiolitic rocks in subsurface. The contact with the Wazhdad volcaniclastics is faulted. Some phylite/schist is observed near the contact zone. The age may be Eocene or late Eocene.
Toe Koh Intrusions (=Washuk Intrusion): Toe Koh intrusion is named after the host Toe Koh just west of Washuk town. The Washuk Intrusion is its synonym. Tow Koh Intrusions are exposed on the southern foot mountain or base of Toe Koh (Washuk-Palatank) mountain Range ( Figure 2). It mostly consists of acidic rocks like granite. The possible age is Eocene or late Eocene.
Makran Group: It is represented by Late Eocene to Oligocene Hoshab and Panjgur formations.
Hoshab Formation: It is named after the village of Hoshab in the Kech valley (31 N/16; [12]). The reference [12] correlated it with the upper part of Murgha Faqirzai shale of north Zhob district. It comprises shale with minor siltstone and sandstone. The lower contact with the Wazhdad formation and upper contact with the Panjgur formation which are conformable. Further [12] correlated the Hoshab shale with the upper part of Murgha Faqirzai shale of northern Balochistan basin and Siahan shale of Wazhdad magmatic arc. According to stratigraphic position, its age is supposed to be late Eocene.
Panjgur Formation: It is named after the Panjgur town (35 B/1; [12]). It consists of alternated sandstone and shale. Sandstone is light green to light grey to grey, fine to medium grained, thin to thick bedded, hard and calcareous. It is correlated with the Mina Formation of north Balochistan basin (Kakar Khorasan basin). Panjgur formation is devoid of fossils in the Panjgur area, however on the west of Panjgur near Iran Boarder, this formation has yielded Oligocene age diagnostic foraminifers [12]. and scalar sedimentary structures such as ripple and groove marks. However the source of the northeastern part of Makran basin seems to be both from northwestern and also from east/Indus Suture due to its close vicinity.
Talar Group: It is named by Malkani [14]. It represents marine Parkini mudstone, Talar sandstone and Chatti mudstone. The Hinglaj series of Vredenburg is considered in this group. Talar Group is well exposed in the South Makran.
Parkini Formation: It is named after the Parkini Kaur, a tributary of the Hingol River (35 G/6) [12]. It consists of mostly poorly bedded mudstone with minor intercalations of siltstone or fine sandstone. The lower contact with the Panjgur formation is abrupt and gradational and upper contact with the Talar formation is transitional. Large fossils are rare while Miocene microforams are prolifically abundant and can be obtained relatively easily from the mudstone, most of which disintegrates readily in warm water. According to microforms and stratigraphic position its age is Early Miocene. Talar Formation: It is named after the Talar gorge (31 K/10) [12]. It is considered equilent to Hinglaj group of [12]. It consists of sandstone, shale, mudstone and shelly limestone. Its lower contact with Parkini and Chatti formations is transitional but at places sharp. The fossils like gastropods (Mollusks) and lamellibranches are common. The microforms are Miocene age diagnostic [12].
The age of the formation is Late Miocene to Early Pliocene.
Chatti Formation: It is after the locality of Chatti (31 K/3) about 17 miles north west of Gawader [12]. It is a part of Makran series paleontologically defined by [84]. It consists of mostly mudstone which is interbedded with siltstone or fine grained sandstone and marl. The Ormara is the synonym of Chatti because Ormara is mapped in the eastern part of southern Makran coastal areas where Chatti formation is not mapped and distinction between Ormara and Chatti mudstone is also difficult in the western part also [12]. Its age may be Pliocene.
Kech Formation: It is named by [12] after the Kech valley near Gish Kaur (Map 9; 31N/8) and Kech Valley generally existed from Hoshab area to Turbat. It is also correlated with Kamerod/ partly Ormara formation. It consists of conglomerate, mudstone and sandstone facies. It also has upper angular contact with Subrecent to Recent surficial deposits. The age of the formation is Pleistocene.
Jiwani Formation: It is named after the coastal village of Jiwani (31 G/12), where it is best exposed. It is synonymous with the "Sub-Recent shelly limestone" and "littoral concrete" [98]. The formation is restricted to the South Makran division of the arenaceous zone and has a thickness upto 100 feet in the type area of Jiwani headland [12]. The formation is composed mainly of shelly limestone, sandstone, and conglomerate. The lower contact with Ormara formation is gradational and placed at the base of lower persistent bed of shelly conglomerate, and at places angular unconformable with Ormara, Parkini and Chatti formations. Its upper contact with the recent deposits or extrusive mud may be angular. The age may be Late Pleistocene to Subrecent [12].
Makran Mudvolcanoes: These are common in coastal areas of Makran but also found in the Pishin Zhob basin particularly near the Qilla Saif Ullah area [12]. It consists of solidified silty and gritty muds. It is soft and friable. In general the mud appears in two forms like cones and ridges. The cones formed by one or more ventral vents. It involves series of eruption and cone is formed from the drying of muds. The ridge type of mud accumulation seems to have no connection with ventral vents or discrete points of eruption but appear as high, broad hill with steep sides and long and parallel with the regional structures. Rutile and methane gas is also present in these volcanoes. Its age may be Sub Recent to Recent.

Mineral Potential of Balochistan Basin, Pakistan: An Update
The reference [99] reported the production from Balochistan Province during 2007-08, 36

Mineral Resources of Northern Balochistan Basin (Pishin Basin or Kakar Khorasan Basin)
Some economic minerals/commodities like antimony, ochre, saline springs, and mud flows with methane-nitrogen gas are found ( Figure 3). Antimony deposit like the stibnite veins are hosted in Khojak group of Qila Abdullah which is 24 km NE of Qila Abdullah town, and smaller deposits in the Qila Viala area 40 km east of Qila Abdullah [5] [12] [13] [100] [101]. Ochre deposits are found in the Shaigalu sandstone of Kaker Khurasan area [9]. Many Saline springs are found in the Qila Saifullah area especially in the Nisai formation. Salt springs running and dry are reported from the red shale at the base of Nisai limestone and so far active mud volcano in the Spara Manda and its vicinity areas of Qila Saif Ullah district (39 B/5.9) [14].

Mineral Resources of Chagai Magmatic Arc
The Chagai arc is economically most important mountain belts of Pakistan. Many important minerals ( Figure 3) including porphyry (Cu-Mo-Au), manto and vein type copper, stratiform and skarn type iron, volcanogenic gold-silver and sulphur, Kuroko type lead-zinc-silver-copper are intimately associated with the magmatic rocks of this arc [102] [103]. The tholiitic and calc-alkaline magmatism in oceanic island arc was reported by [102] [103] while before this it was considered as Andean type (continental) calc-alkaline magmatic belt.
Copper: The copper deposits and showings occur extensively at several localities in the Chagai magmatic arc [12] [102]- [109]. There is a moderate to weak K zone and the hypogene mineralization has developed in two phases, the first phase produced pyrite, chalcopyrite, enargite and pyrrhotite and the second one introduced magnetite, molybdenite and chalcopyrite [103]). Three bore holes have been drilled in western stock. Average copper values in quartz sericite zone vary from 0.1% -0.17% and in the potassium silicate zone from 0.25% to 0.54%. The breccia pipe zone in the eastern stock contains surface values upto 4.5% copper but not drilled [8]. Talaruk copper deposit is 64 km NW of Saindak in Chagai District. It is a massive Kuroko type deposit and mineralization is of submarine exhalative origin. The copper ore occurs in two zones, one in rhyolite intrusives in which chalcocite is the main copper mineral and the other in volcanic breccia associated with gypsum, with malachite as the main copper mineral. Six bore holes were drilled at this deposits and its copper content has been about 0.65% [110].
Saindak copper deposit is located about 9.4 km SE of Fort Saindak (29˚18'N; 61˚33'E) in Chagai district. The ore is hydrothermally altered and the mineralized zone is known as Saindak alteration zone [111].  Gold-Silver: The production of copper along with gold will be started soon from Saindak porphyry copper deposits. GSP has discovered a number of porphyry copper deposits with gold and silver mineralization [114]. Telethermal vein type and skarn deposits are also reported. Broken Hill Propriety (BHP) of Australia in collaboration with BDA has discovered world class gold deposits. Lake Resources (Australia) also explored copper and associated gold deposits and their alteration zones [8].  [117]. There are 27 small magnetite-hematite bodies at this area. At Pachin Koh 62 holes, where as 29 holes in Chigendik drilled. The estimated ore reserves of Pachin Koh are 45 mt and of Chigendik is 5 mt of which 30 mt are proved. The geological and geophysical investigations show that the deposit may be increased upto 100 mt. Steel mills process this ore with 46% substitute of the imported ore. The reference [118] has suggested the ore is suitable for direct reduction plus electric arc furnace process combination. This process can produce steel billets at about 30% lower cast. Chilghazi iron deposits are located 52 km NW of Dalbandin town. The area is underlain by Cretaceous Sinjrani volcanics, which are intruded by small bodies of diorite, quartz monzonite and granodiorite. The deposit sis found in Sinjrani which forms asymmetrical gently dipping anticline. The iron ore is comprised of massive magnetite and layers of disseminated magnetite. The ore occurs at three horizons. The upper one near the top contains main deposits. The other two are 166 and 500 m below the first one. The lower ore bodies are largely comprised of magnetite disseminations in volcanic rocks and are lean in their iron content (10% -12%). The deposit has been drilled and indicates the main ore body contains iron 32% -52% (average 45%), copper 0.1% -1.96% (in one hole upto 7%), phosphorous upto 0.1%. Some portion of the ore body contains upto 1 oz/ton of gold [13] [119]. It has high grade ore with 3.36 mt (2.46 proven and 0.90 probable). The low grade reserves with 25% -30% iron are estimated 20 mt [120].
Tungston: The tungsten ore has been recorded by [121] [122] from Amalaf  [13]. Copper is reported from Tor Tangi of Ras Koh areas [104]. Various types of limestones and igneous rocks can be used for this construction and decorative stones.

Mineral Resources of Wazhdad magmatic arc
The recently discovered Wazhdad magmatic arc [14] [18] [96] hosts the ophiolitic and volcaniclastic rocks in the Wazhdad-Toe Koh and its vicinity show minor chromite, copper, soapstone and asbestos mineralizations ( Figure  3). Granite of Washuk ophiolite is best for dimension and décor stones, besides this the best green to grey tuffaceous rocks of Wazhdad range are also significant for cu mineralization, decorative and dimension stones resources. Antimony showings are also found. Pl. see detail in the Siahan Range description as below.
Mineral Resources of Hamun Mashkel basin (inter arc basin) The Hamun Mashkel basin includes the exposed eolian sands, alluviam gravel, conglomerate and sands. It subsurface may have coal or any significant lake deposits.

Mineral Resources of Makran and Siahan basin (Arc-Trench gap basin)
The reference [14] [16] [17] reported first time some new findings of Makran and Siahan ranges ( Meteorites: The reference Malkani [14] [16] [17] has reported possible meteorite first time in Pakistan, discovered from Soro and Phudkush area (35 A/3) (Figure 2) about 1 -2 kms toward south from the main track/road or east west jeepable track of Washuk to Panjgur (or Pajgur to Washuk). These meteorites are found in Eocene-Oligocene Siahan shale. These meteorites are represented by one big iron body just like a room sized big boulder with nearby one or two minor boulders located a few meters westward. These iron boulders have no relation to host rocks and seems to be meteorites. It is a hematite with green weathered colour. Coal, carbonaceous shale and carbonaceous sandstone: Coal, carbonaceous shale and carbonaceous sandstone are observed in the Ahurag area (31 M/12) (Figure 2). It is 90 km northwest from Panjgur town. The thickness of coal and carbonaceous sandstone is 4 cm on the eastern side of Ahurag Kaur. On the western side of Ahurag Kaur 3 further layers of coal, carbonaceous shale and carbonaceous sandstone are observed. The extension of these coal seams is not known. Coal and carbonaceous shale is also reported by [12] from the Hoshab/Balgor area. However Balochistan desert is also important for exploration of lagoonal and lacustrine coal.  [14]. Mud volcanoes of cold muddy water also show anomalous gas like methane upto 74.5% and nitrogen upto 13.8% near Ormara [12]. Many salts deposits and lakes are located in the vicinity of Makran coast and Hamun i Mashkel area. Alum may also be associated with these salts [14].

Revised Stratigraphy and Mineral Resources of Western Indus Suture (WIS; Contact of Balochistan Basin: A Part of Tethys and Indus Basin: A Part of Gondwana Southern
Hemisphere) The western Indus suture is a suture between the Balochistan basin (a part of Tethys) and Indus Basin (an aprt of Gondwana). The western Indus suture is jointed just east of Balochistan basin that is the reason being described here. It includes the ophiolitic mélanges and sedimentary Mesozoic and Cenozoic sedimentary sequences. Revised Stratigraphy of Western Indus Suture (WIS Lasbela-Khuzdar Quetta-Muslimbagh-Zhob-Waziristan), Pakistan: The Bela Volcanic Group is 190 km long and 20 km wide, extending from Ornach in the north to Windar in the south. Volcanic rocks are subordinate in the north of Ornach and dominate in the south. It consists of intermixed volcanic and sedimentary rocks. The volcanic rocks are mainly basalt, lava, coarse grained agglomerate and bedded tuff. The lava flows are commonly pillowed and spilitic. Most of the weather reddish brown or green, but the more massive types weather black and are difficult to distinguish from intrusions [12]. Rocks are altered and fractured filled with epidote and carbonate. Phenocrysts of augite with rims of chlorite are common, amygdules of calcite and microlites of feldspar are abundant. Interlayered sediments are shale, marl, limestone, conglomerate, and radiolarian chert. This group overlies the Windar group conformably (west of Mor range), and is overlain unconformably by the Oligocene Nal limestone (Northwest of Bela). Its age is Cretaceous [12]. Bela Ophiolite Complex consists of mainly ultrabasic, basic, and intermediate compositions. Granitic rocks are rare. The true granite is in the form of conglomerate pebbles. The ultrabasic rocks are altered pyroxenite, serpentinized peridotite and amorphous and sheared serpentrinite. The rocks of intermediate compositions are diorite and gabbro. The gabbro is dark green rock spotted with large crystals of white feldspar which is kaolinized. Some types are pegmatitic and exhibit crystals upto 4 inches across of biotite and pyroxene. A small body of the granodiorite located in the west of Porali river, 10 km south of Wad. Concordant and discordant intrusions are found. Iridescent soapstone found from Nal area. Muslimbagh Ophiolite Complex consists of mainly serpentinized ultrabasic rocks that include saxoniter, dunite and pyroxenite. It also consists of dolerite, gabbro, and diorite but these seem slightly later phase. The age is Late Cretaceous-Early Paleocene [12] [133]. Geological formations associated with igneous rocks are widely (10 km) exposed in the Indus Suture The extension of present pitting shows much more reserves than above mentioned. Zhob area chromite (Zhob District) is close to Zhob town in the north. Chondrite is a stony meteorite contains chondrule (small rounded bodies of olivine or enstatine) embedded in a fine grained matrix of pyroxene, olivine and nickel-iron [148].
Asbestos: Small deposits and showing of chrysotile and tremolite asbestos are found in serpentines of the ophiolitic complex near Naweoba (Zhob) [5], Taleri Mohd Jan (Muslimbagh) [5] and Wad Khuzdar. where as the sulphide mineralization is syndiagenetic and formed by displacement or replacement of the host siliceous fluids. Deformation of sulphide layering shows that ore was formed before early emplacement and there fore preTertiary. Proved reserves of 6.38 million ton/mt and inferred reserves 3.43 mt with 11.34% Zinc and 2.01% lead have been established [145]. The Gunga deposit, 11 km SE of Khuzdar, is hosted by Early to Middle Jurassic Anjira Formation. The mineralization is stratiform, stratabound, open space filling type. The zone extends over a distance of 1200 m and easily distinguished as silicic gossans. The gossans contains 3% -4% Pb and Zn. The deposit was explored through 14 drill holes. The ore body contains over 6% Zn and 1.5% Pb, with proven reserves of 6.5 mt, probable reserves of 3.0 mt, and possible reserves of 3.3 mt [139] [143]. The Surmai deposit is located 1 km South of Gunga depo-sit and hosted by Loralai Formation and is of Mississippi valley type. It has been explored by GSP and JICA and reserves of 2.93 mt of ore with average content of 6.5% have been established. This deposit also contains 10 -20 gm/tone of Silver [146] [149].
Manganese ore: Manganese deposits occur as marine, chemically precipitated sedimentary ores, as secondary enrichment deposits and as hydrothermal deposits. The deposits of manganese ore in Pakistan are associated with volcanic rocks in the ophiolitic thrust belt [150]. In the Bela ophiolitic thrust belt, lenticular manganese ore bodies occur in ferruginous and siliceous horizons overlying basaltic pillow lavas. The more important localities are Kharari Nai are associated with heavy minerals (for example in India) like ilmenite, sillimanite, garnet, zircon, monazite and rutile, collectively called beach sand minerals (BSM). The Balochistan Basin has a long east west trending coastal belt and oceanic beach sands and oceanic clay in the southern Makran in which REE can be explored. Further the pink coloured beach sand is common in sea coast of Balochistan basin like Gawader pink beach sand which is indication of zircon, monazite and other heavy minerals.
Global and national Geoparks installation in Balochistan basin and western Indus Suture, Museum and Geo-assets: Balochistan Basin is represented by Cretaceous to Recent Tethys geoheritages [12] [156]- [165], while other regions of Pakistan host Gondwanan as well as Laurasian geo-heritage. Balochistan Basin includes significant diverse mineral rsources hosted by diverse sedimentary, igneous and metamorphic rocks. Balochistan basin hosts mud volcanoes and meteorites unique in Pakistan and other geo-assets which needs protection of these paleogeoheritage as national and global geoparks which is an innovation for the sustainable development of science and Pakistan. A new island was emerged during the 1945 earthquake [166], mud crater extrusion [167] and deformation of Makran coast [168]. Previously most of the Balochistan basin was considered flysh marine deposits but now the northern part of Kakar-Khorasan basin (northern Balochistan basin) yielded terrestrial rhinoceroses Pakitherium shagalai [80] [81] [82] from Eocene Shagala Formation of Shagala Group located in Shagala-Kamardin Karez area of Zhob district, Balochistan Province, Pakistan. The fossils of these rhinoceroses [80] [81] [82] from Balochistan basin, and titanosaurian sauropods [169] [170] [171] [172] and theropods [173], mesoeucrocodiles [173], pterosaurs [173] and other recently discovered biotas [82] found from Pakistan are hosted in museum of the Geological Survey of Pakistan, Quetta, Balochistan. Further the sites of Mesozoic diverse footprints/tracks and trackways of diverse dinosaurs [82] [174] [175] need their protection.

Conclusion
Balochistan basin consists of Cretaceous to recent sediments, diverse igneous rocks and low grade metamorphics. Balochistan basin is a leading basin which consists of very significant mineral deposits especially copper (associated some gold, silver, molybdenum). Some commodities are being utilized and exploited but most of the commodities are waiting for their utilization and developments for the area, Balochistan and ultimately for the development of the Pakistan.

Conflicts of Interest
The author declares no conflicts of interest regarding the publication of this paper.