The Rich Gol Metamorphic Complex: evidence of separation between Hindu Kush and Karakorum (Pakistan)

0 Acadbmie Tectoncs /

des sciences

Tectonique

/ Elsevier. Paris

The Rich Gol Metamorphic Complex: evidence of separation between Hindu Kush and Karakorum (Pakistan) Le complexe mbtamorphique du Rich Go/ : &icience de dparation entre /‘Hindu Kush et le Karakorum (Pakistan) Andrea

ZANCHT’*,

Maurizio GAETANI,~ and Stefano

POLIO

’ Dipartimentodi Scienzedellilmbiente e de1 Territorio, Via Emanuelr 15, 20126hfilano; ’ Dipatiimentodi Scienzedellu Tevu, Viu Mangiagalli 34. 20133Milano; ’ Dipartimentodi Scienze della Terra, Via Botticelli, 23, 20133 Milano, Ita!)

The westernmost part of the Karakorum belt and its prosecution along East Hindu Kush includes: 11 the southern portion of the Tash Kupruk Unit; 2) the Shah Jinali Phyllites; 3) the Rich Go1 Wztamorphic Complex (RGMC). a narrow belt of high-grade metabasites with serpentinites and metapelites, which forms a narrow strip along the Tirich Mir Fault, separating the Atark Unit (Hindu Kush?) from Karakorum metasediments. The RGMC may represent the easternmost part of similar complexes described around the Tirich Mir and may be linked to the boundary between Karakorum and East Hindu Kush. Keywords:

Pakistan, Karakorum.

East

Hindu Kush, Metabasites. Serpentinites, Tirich Mir Fault

La marge occident&e du Karatbum Pakistanais et sa prolongation dans L’Hindu Kush oriental est constituee de plusieurs unit&s tectoniques, dont certaines sont d&rites ici pour la premitirefois Ii l’unitk Tash Kupruk; 21 la formation desphyllites du SbahJinali ; 3) le complexe m&amolphique du Rich Go1(RGMCI. une bande de mgtabasites et de m&tap&tes de haut grade in&ant des wpentinites en bande etroite le long de la,faille du Tirich Mir, qui skpare 1’unitB carbonatke d’iltark (Hindu Kush 9 des mt?tas@dimentsappartenant au Karakorum. Les mktabasites reprt%ententprobablement leprolongement leplus oriental des complexes similaires d&r&s dans la r&ion du Tirich &fir Ce.7comp1exe.ysemblent marquer h limite entre le.7deux chaines. Mots cl&

: Pakistan,

Karakorum.

Hindu

Kush, M&abasites,

Serpentinites,

Faille du Tirich Mir

VERSION ABR~G~E Les liaisons entre chaines de montagnes du Karakorum et de 1’Hindu Kush oriental sont encore i dechiffrer avec precision (figure 1). Au NW Pakistan dans le haut Chitral, de la vallee du Rich Go1 jusqu’au co1 du ShahJindli, il existe un secteur qui n’a

jamais et6 6tudi6 jusqu’alors et qui est fondamental pour comprendre les rapports entre les deux chaines. Le Karakorum occidental est form6 de grands batholites d’3ge C&a& moyen, &par& les uns des autres par des m&a&-

Uote pr&ent6e parJean I)ercourt

’ E-mail: Zanchllalpha disat.unimiit C. R. Acad. Sci. Paris. Sciences 1997. 325.877-802

de la terre et des plan&es

/ Earth & Planetary Sciences

877

A. Zanchi et al.

merits faiblement metamorphiques (Pudsey et al.. 1985 ; Gaetani et al., 1996). Au nord des complexes piutoniques, affleure une serie d’unites structurales essentiellement sedimentaires, peu ou non m&amorphiques. Du sud-est au nord-ouest (IFgure 11, on rencontre les unit& suivantes : - 1) Unit.@ uxiule (Gaetani et al., 1996) : mCtasCdiments terriggnes. surmont& de roches carbonatkes du Permien, recouverts en discordance par le conglom&at de Reshun (Hayden, 19151, d’age Cretace ; - 2) Unity & Las& (Gaetani et al.. 1996) : elle comporte plusieurs ecailles tectoniques, et est formee par la succession de lits terrigenes et de carbonates massifs et stratifies (D&onien moyen-suptrieur-Permien) ; - 3) 1JnitP de ?‘ash KupruIz (Kafarskyi et Abdullah, 1976) : dolomies massives claires, basaltes et volcanoclastites 2 tr& bible mktamorphisme (Gaetani et al., 1996) ; - 4) Pbyl1ite.sdu Shah Jinali (unite cr&e dans cette note) : succession de phyllades et quartzites, qui ont subi au moins deux episodes de deformation, une foliation Sl soulign& par le litage de muscovite, chlorite, quartz et porphyroblastes de grenat et de chlorito’ide, suivie par une deformation S2 avec plis se&s et clivage de cr&ulation vertical. - 5) Complexe mdtumotphiyuc du Rich Go1(RGMCI : la d&ouverte et la description des types lithologiques majeurs de ce complexe constituent le point central de cette note : certaines de ces roches avaient tte signalees ailleurs dans le Chitral, par Huchroithner et Gamerith (1986) et Gaetani et Leven il993), mais aucune conclusion geologique n’en avait et6 tiree. Le RGMC est form& d’amphibolites. de mi-tapelites, et d’ukramafites serpentinisees. Les amphibolites sent reprt%entees par des amphibolites granoblastiques i amphibole. plagioclase et quartz; des amphibolites Sipyroxene en gros cristaux; des schistes mafiques g faci& schiste vert et des amphibolites g amphiboles zonkes blewvert. Les metapelites sont repr&entPes par ties mt?tapelites migmatitiques, avec feldspaths-K microperthitiques + plagioclases + quartz + sillimanite fibrolitique, et des m&apelites i facies amphibolite, avec staurotide + grew + biotite + musctwite + quartz.

Les ultramafites : les roches serpentinisees sont toujours trPs schistosees, mais contiennent par endroit des reliques d’olivine et de clinopyroxPne. Des roches equivalentes ont ttk d&rites au sud-ouest du pluton du Tirich Mir, dans la vallee de Arkari (Buchroithner et Gamerith, 1986) ; elles forment aussi la roche encaissante du pluton. - 6) Unite d’Atu& (Buchroithner, 1980) : c’est une succession tr& epaisse de roches carbonatees massives, peu ou non m+tamorphiques. Les Hges s’&alent du Permien inferieur (Gaetani et Leven, 1993) au Trias. et peut-@tre au C&a&. Une molasse rouge semblable aux conglom&ats du Tupop du Karakorum septentrional (Gaetani et al., 1993) complete la succession sedimentaire. - 7) Schistes du U%$han (Hayden, 1915) : il s’agit d’une puissante succession de schistes et de gr?s, i m&amorphisme faible, d’sge essentiellement Pali-ozo’ique. Les conclusions qui peuvent &tre tirees de cette exploration p&liminaire sont les suivantes. Les roches du RGMC soulignent un metamorphisme de degre gleve. Des roches tr& variees et des associations mktamorphiques diverses sont regroup6es dans le RGMC. Des temperatures supCrieures a 800”-850” C et des pressions comprises entre 3-4 et 10 kbar peuvent &tre envisagees, suivies d’un r&rom&amorphisme de facies schiste vert. Le RGMC forme une bande mince le long de la faille de Tirich Mir et peut etre suivi dans la meme position structurale, sur une distance superieure ZI 150 km, du nord-est au sud-ouest du Tirich Mir. Le RGMC, d’aprPs les auteurs (Huchrotiner et Gamerith, 19861, semble Etre coupe par le pluton du Tirich Mir. dont on a citC un rige C&a& (Desio et al., 1964). La presence du conglomPrat de type Tupop dans l’unite d’Atark suggere que les histoires de 1’Hindu Kush oriental et du Karakorum ont &C semblables apr?s le C&ace. Le RGMC est done un candidat majeur pour localiser la limite entre les chaines du Karakorum et de 1’Hindu Kush oriental. hmite qui doit se trouver, en tout cas. entre l’unite du Tash Kupruk et la faille du Tirich Mir.

Introduction

Geologic Pakistan

The geological relationships between Karakorum and E Hindu Kush in NW Pakistan (figures 1 and 2) are still largely unexplored (Searle, 1991; Caetani and Leven, 1993; Searle and Khan, 1966; Gaetani, 1997; Zanchi et al., 1997; Khattakh et al., 1997). North of the structural units defined by Gaetani et al. (1996) in the Yarkhun Valley, a narrow belt of high-grade metamorphics, here named the Rich Gol Metamorphic Complex (RGMC), has been detected during a 1996 geological expedition from the Yarkhun Valley to the Rich Gol. The RGMC lies along the Tirich Mir Fault and is sandwiched between the Hindu Kush (?) Atark Unit (Buchroithner and Gamerith, 1986; Gaetani and Leven, 1993), and low-grade phyllites and slates belonging to Karakorum.

878

C. R. Acad.

setting (Chitral)

of north-western

According to Gaetani et al. (1996) and Caetani (1997), the region (figure 2), between the Atark Unit to the north and the Northern Suture (Pudsey et al., 1985) to the south, represents the western part of the Karakorum Belt. The Reshun Fault (RF), a major NE-SW trending SW-vergent thrust, crosses this part of Karakorum, juxtaposing a mainly Paleozoic unit over Paleozoic and Mesozoic rocks. The footwall of the RF consists of the Late Cretaceous Reshun Formation, unconformably covering a complex belt including westward the Koghozi Greenschists, the Chitral Slate, the Krinji and the Gahiret Limestones, Jurassic and Cretaceous in age (Desio, 1963, 1966; Pudsey et al., 1985) and eastward the Paleozoic-Mesozoic

Set. Paris, Sciences

de la terre et des pIaMes

/ Earth & Planetary Sciences 1997. 325,077~882

The Rich Gol Metamorphics:

western boundary

of Karakorum?

Figure 1. Structural map of NW Pakistan, from Pudsey et al. (19851, Buchroithner and Camerith (19861, Gaetani and Leven (1993), Gaetani et al. (1996), Searle and Khan (1996). SS: Main Mantle Thrust; NP: Nanga Parbat; NS: Northern suture; RPS: Rushan-Pshart suture; WABS: Wanch-Ak Baital suture. 8-r*.tx Carte structurale du Nord-Ouest du Pakistan. Gaetani et al. (7 996), Sear/e et Khan (1996). WABS I suture Wanch-Ak Baital.

ModiMe 5.5’ : Main

d’apr& Mantle

Pudsey et al. (19851, Buchroithner et Gamerith (1986), Gaetani et Leven (1993), Thrust; NP : Nanga Parbat; NS : suture du Nord; RPS : suture de Rushan-Pshart ;

metasediments of the Darkot Unit and the Late Paleozoic metasediments of the Axial Unit of Gaetani et al. (1996). Three distinct belts of deformed granitoids, separated by metasediments, occur along the southern border of the described units. In the western part of the area, the hanging wall of the RF consists of Devonian rocks (Lun Shales and Shogram Fm; Desio, 1963; Talent et al., 1981), and Permo-Triassic limestones. Buchroithner and Gamerith (1986) describe, south of Tirich Mir, slates and phyllites with Devonian limestones, quartzites, volcanics and volcaniclastics, named Owir Series, in part correlatable with the Lun Shales. In the central sector (Tirich Gol) the metapelitic C. R. Acad. Sci. ParIs, Sciences 1997. 325.877-882

de la terre et des plan&es

successions (Lun Shales?) are separated by the Tirich Mir Fault (Buchroithner, 1980; Buchroithner and Gamerith, 1986) from the Permo-Mesozoic carbonatic Atark Unit (Gaetani and Leven, 1993), cropping out northward. East of the Tirich Gol four different units have been recognized between the RF and the Atark Unit: 1) the Lasht Unit; 2) the Tash Kupruk Unit; 3) quartzite-bearing metapelites (Shah Jinali Phyllites); 4) a metabasitic complex with minor amounts of serpentinites and metapelites (Rich Gol Metamorphic Complex: RGMC). North of the Atark Unit, the mainly Paleozoic Wakhan Slates (Kafarskyi and Abdullah, 1976; Buchroithner, 1980) occur. The Wakhan Slates, which overthrust the Atark IJnit, are intruded to the north

/ Eaarth & Planetory

Sciences

879

A. Zonchi

et 01

Figure 2. Geologic Carte

g&o/ogique

map of the upper Rich Gol area. ID: lsperu Dok; SC: Shah Chard. de la r&ion

by the East Hindu

du Rich

Gol.

Kush granitoids.

Mir Pluton, at., 1964).

records

a Rb-Sr

Geology

of the Upper

One

Dok

of these,

age of 115 + 4 MA

; SC : Shah

the Tirich (Desio

et

Rich Gol

From the Yarkhun Valley to Morich tectonic units have been recognized Axial

ID : lsperu

(figure 2) the following from SE to NW:

The Axial Unit (Gaetani et al., 1996) forms the footwall of the RF and includes Permian limestones unconformably covered by the Reshun Fm, consisting of red marls and siltstones followed by coarse polymictic conglomerates. Intensive deformation of these rocks is suggested by tight folding, pervasive cleavages and local transposition. Lasht Unit

left bank

880

of the Siru Gol,

stacked sheets.

a terrigenous/carbonatic

above Along

the the

succesC. R. Acod

sion (Shogram Fm, Middle-Upper Devonian) is overthrusted by sandstones of the Gircha Fm, forming a SEvergent recumbent syncline. The highest thrust sheet consists of marls and massive limestones, forming a broad anticline cut by ENE-WSW sinistral strike-slip to oblique faults.

Tash Kupruk

Unit

This unit (Gaetani et al. 1996) is directly Reshun Fault and includes three thrust

Gharil.

Unit

The Tash Kupruk Unit (Kafarskyi and Abdullah, 1976; Gaetani et al., 1996) consists of Late Devonian-Early Carboniferous basaltic lava flows, volcaniclastics and carbonates. Lavas often preserve igneous textures; phenocrysts of clinopyroxene occur in a groundmass of plagioclase, magnetite, and aphyric material. Low greenschist facies metamorphism affects these rocks, with development of chlorite, epidote and, occasionally, actinolite. lsoclinal E-W folds and complex superposed folds affect the carbonates of the Tash Kupruk Unit at lsperu Dok and Lasht. The main structures of the unit trend Yarkhun Valley to the Shah Jinali Pass; south

Sci. Paris, Sciences

de lo terre et des plan&es

/ Earth

E-W from the of the pass the

& Planetary

Sciences

1997. 325.077482

The Rich Gol Metamorphics: unit is significantly the divide between Shah jinali

rotated assuming a NE-SW trend the Siru and Shah Jinali valleys.

along

A succession of dark-greenish phyllites with quartzites crops out between the Tash Kupruk Unit and the RGMC southwest of the Shah Jinali Pass along the Shah Jinali and Rich valleys. This unit, here described for the first time, consists of greenschist-facies metapelites represented by garnet-, chloritoid-phyllites with chlorite, muscovite, and quartz. An Sl foliation is defined by muscovite, chlorite, and quartz layers with garnet and chlorithoid porphyroblasts; kink bands, tight folds and a strong vertical crenulation cleavage defined by stilpnomelane needles (S2)

The Rich Gol Metamorphic The Rich Gol Metamorphic includes: 1) amphibolites; nized ultramafics.

Complex

near faults

Complex (figures 1 and 2) 2) metapelites; 3) serpenti-

a) granoblastic having a roughly amphibolites, equigranular association of subhedral amphibole, plagioclase and quartz, with interstitial magnetite and titanite. Such rocks show minor greenschist-facies reequilibration; b) coarse grained pyroxene-amphibolites, with reaction symplectites of pyroxene and amphibole. Large euhedral crystals of green-brown hornblende are largely affected by overgrowths of pyroxene lamellae, which suggest a prograde breakdown of amphibole at low stress conditions; c) mafic schists, the most common fine grained foliated amphibolites, mainly consisting of hornblende, plagioclase and quartz, with a variable extent of greenschist-facies retrogression recorded by tremolitel actinolite, chlorite and epidote aggregates; d) ‘blue-green’ amphibole-bearing mafic rocks, with a peculiar zoning of amphibole up to a ‘blue-green’ amphibole, possibly barroisitic in composition. 2) Metapelites a) ‘migmatitic’ metapelites, characterized by microscopic segregates of perthitic K-feldspar, plagioclase, quartz and ‘refractory’ felts of both prismatic and fibrolitic sillimanite developed on relics of red-brown biotite. Submillimetric garnet is homogeneously distributed in the rock. Muscovite only occurs when alkali-feldspar is absent and sillimanite is fibrolitic, suggesting a somewhat lower temperature of metamorphism. Layers of inequigranularamoeboid quartz further indicate a process of hightemperature annealing of previously foliated rocks; b) amphibolite-facies metapelites, mostly micaschists composed of a typical staurolite + garnet + biotite + muscovite + quartz assemblage. A polydeformational history

C R Acad. Sci. Paris, Sciences 1997. 325,877.882

de la terre et des planetes

and

fol-

only Mafic

locally schists

and amphibolite-facies metapelites occur in the Uzhnu Gol, whereas the other rocks have been found between Shah Jinali and Rua. The RGMC thus displays remnants of a prograde temperature path and a complete sequence of retrogressive metamorphism. Upper pressure conditions are substantially constrained by the absence of epidote in textural equilibrium with hornblende and plagioclase in the metabasites and by sillimanite in the metapelites. Maximum temperatures are constrained by the breakdown of biotite to K-feldspar + sillimanite + garnet (+ melt?) and by the breakdown of hornblende to pyroxene. Both facts suggest that RGMC necessarily attained temperatures higher than

1986)

this

unit

consists

gabbros, diorites, and hornblendites ized serpentinites. Tirich

1) Amphibolites

of Karakorum?

3) Ultramafics

800-850 “C at pressures higher than 3-4 than 10 kbar. In the Tirich Mir area (Buchroithner

(RGMC)

is recorded by biotite porphyroclasts in microlithons, lowed by a gentle crenulation and folding.

boundary

Serpentinites are always very schistose contain relics of olivine and clinopyroxene.

Phyllites

deform previous foliation. F2 folds trend NE-SW Morich and in the Uzhnu Gol. Sinistral strike-slip have also been observed around Shah Gharil.

western

Mir

The Atark

and

of

medium

kbar,

but lower

and

Camerith,

to coarse-grained

foliated to banded gabbro-amphibolites metamorphosed into strongly tectonThis NNE-SSW belt occurs just west of it is intruded

by the Tirich

Mir

pluton.

Unit

The Atark Unit consists of Permo-Triassic carbonates with slates at the base (Buchroithner,l980; Gaetani and Leven, 1993). The Atark Unit extends from the Arkari Gol west of Tirich Mir to the Yarkhun Valley a few km east of Lasht. The unit is bounded to the south by the Tirich Mir Fault and it is intruded by the Tirich Mir and by the Rich Gol Plutons. The metabasites of the RGMC are always bounded to the north by this unit, which is in turn overthrusted by the Wakhan Slates. Important tectonic repetitions due to thrust stacking and polyphasic folding are exposed along the Shah Jinaly and Rich valleys, where mountain-scale NNE-SSW to NE-SW trending recumbent folds in part associated with SE-vergent thrusts occur. A few km down from Shah Jinali, strongly deformed reddish conglomerates have been found within the Atark Unit along a high-angle reverse fault. This conglomerate strongly resembles the Cretaceous Tupop Fm of the Hunza Karakorum (Gaetani et al., 1993), or the conglomeratic facies of the Reshun Fm. The Rich Gol Pluton A small undeformed granodioritic upper part of the Rich Gol north

pluton crops out in the of Purgram and Rua. Large dikes and small stocks, coarse-grained contact marbles and low grade metapelites suggest that it was emplaced within the Atark Unit at low depth.

Conclusions l-The RGMC indicates a sharp jump with respect to the surrounding units.

/ Earth & Planetary

Sciences

in metamorphism

881

A. Zonchi et al. 2-The RGMC includes high grade metabasites and metapelites with highly deformed serpentinites in the Rich and Shah Jinali Gol, to staurolite micaschists and fine grained amphibolites with a greenschist-facies retrogression in the Uzhnu Gol. These rocks suggest maximum temperature conditions higher than 800-850°C and pressures between 3-4 and 10 kbar followed by a retrogression to greenschist-facies. 3-The RGMC forms a thin slice along the Tirich Mir Fault, which can be followed in the same structural position for a long distance, from the end of the Tirich Gol to the Shah Jinali Pass. The RGMC may be linked with similar rocks cropping out west of Tirich Mir (Buchroithner and Camerith, 1986) for a total extent of more than 150 km. 4--The high-temperature metamorphics of the RGMC and the occurrence of basic and ultrabasic rocks may represent a possible element of separation between Karakorum and

East Hindu Kush, whose boundaries are still questionable (Sear/e and Khan, 1996; Gaetani et al., 1996; Gaetani, 1997). %-According to the map of Buchroithner and Gamerith (1986), tectonic coupling of the Atark Unit and of the metabasites occurred before mid-Cretaceous, as suggested by the age of the Tirich Mir Pluton, which intrudes both units. 6-The presence of Tupop- or Reshun-like ‘molassic’ conglomerates (Cretaceous?) in the Atark Unit north of the RGMC may suggest a common history for the Karakorum and East Hindu Kush blocks at least since that period. In conclusion, the boundary between Karakorum and the East Hindu Kush Range should lie in the belt between the Tirich Mir Fault, the RGMC and the Tash Kupruk Unit. At present, we may suppose that some major points are in favour of placing the actual boundary at the RGMC.

Buchroithner M.F. 1980. An outline of the geology of the Afghan Pamirs, Tectonophysics. 62, 13-35 Buchroithner M.F. and Gamerith H. 1978. Geological map of Pamir-e-Wakhan. 1:250.000. In Grosser Pamir. De Granchy R S. and Kostka R. (eds), Enclosure, Graz (Akad Druck- und Verlagsanstalf~ Buchroithner M F. and Gamerith H. 1986. On the geology of the Tirich Mir area, Central Hindu Kush (Pakistan). Jb. Geol. B.-A.. 128, 367-38 1 Desio A. 1963. Review of the geological ‘formations’ of the western Karakorum (central Asia), Riv. It. Paleonto/. Strut., 69, 475-501 Desio A., Tongiorgl E. and Ferrara G 1964 On the geological age of some granites of the Karakorum. Hindu Kush and Badakhshan (Central Asia), Proc. 22nd Internat. Geol. Congr. De/hi, Pt. 11, Sect. 1 1,479.496 Desio A 1966. The Devontan sequence in Mastuj valley (Chltral, N.W Pakistan), Riv. it. Paleonfol. Strut., 72293-320 Gaetani M. 1997 The Karakorum Block in Central Asia, from Ordovician to Cretaceous. Sediment. Geof., 109,339.359 Gaetani M. and Leven H 1993. Permian stratigraphy and fusullnids from Rosh Gol (Chitral, E Hindu Kush). Riv. It. Paleonto/. Sffuf.. 99,307.326 Gaetanl M , Jadoul F, and Garzanti E. 1993 Jurassic and Cretaceous erogenic events in the North Karakorum: age constraints from sedimentary rocks, In: Himalayan tectonics, Treloar P.J. and Searle M.P (eds). Geol. Sot. Spec. Pub/.. 74,39-52 Gaetani M., Le Fort P,, Tanoli S., Angiolini L.. Nicora A., Schunnach

D. and Khan A, 1996. Reconnaissance geology in Upper Chitral, Baroghil and Karambar districts (northern Karakorum, Pakistan), Geol. Rundsch.. 85.683-704 Gamerith H. 1982. Geologische Karfe van Gi/git/ Chitra// Whakhon (North Pakistan und Ost Afghanistan) 1.250.000, Prrvate Edition, Graz Hayden H.H. 1915. Notes on the geology of Chitral. Gilgit and the Pamirs. Rec. Geol. Surv. Pakistan, 8.2, 1-28 Kafarskyi K.A. and Abdullah J. 1976. Tectonics of north-east Afghanistan (Badakhshan, Wakhan, Nurestan) and relationships with the adjacent territories, A#i Convegni Lincei, 2 1, 87-113 Khattak M.U.K.. Khan S. and Ahmad W. 1997. Tirich Mir Fault Zone of Chitral, Northern Pakistan, XII Himalaya-Karukorum-Tef Internafional Workshop, Rome 16 1&3/4/!997, Abstr, Vol., 167 Pudsey C.. Coward M.P., Luff I.W., Shackleton B.F, Windley B.F. and Jan M.Q. 1985. Collision zone between the Kohistan arc and the Asian plate in NW Pakistan, Trans. Roy. Sot. Edinburgh, 76. 463-479 Searle M.P. 1991, Geology and tectonics of the Karukoram Mountains. John Wiley and Sons, 358 pp Searle M.P. and Khan A. (eds). 1996. Geological map of North Pakistan, 1650.000. Blackwell, Oxford Talent J.A.. Conaghan P.J.. Mawson R.. Molloy P.D. and Picketi J.W. 1981. Intricacy of tectonics in Chitral (Hindu Kush). Fauna1 evidence and some regional implications, Himulayon Seminor (1976). section /IA, Geol. Sun/. India, Misc. Pub/. ,4 1, 77-10 1 Zanchi A., Gaetani M., Angiolini L., De Amicis M. and Poli S. 1997. The 1:150,000 new digital geological map of the North Karakorum Terrain from the Chapursan Valley to the Morich Gol (Northern Pakistan), XII Himalaya-Karakorum-Tibet Infernotional Workshop, Rome 16 1B/4/ 1997. Abstr. Vol ,239-240

082

C. R. Acad.

Sci. Paris, Sciences

de la terre et des plan&es

/ E&h

& Planetary Sciences 1997. 325.877-882