Chapter 24A. Summary for the Mineral Information Package 

for the Nuristan Rare-Metal Pegmatite Area of Interest

Contribution by Mark D. Cocker

Abstract

Numerous rare-metal pegmatites are found in the mountainous terrain of the Hindu Kush in 

northeastern Afghanistan. Earlier investigations by Soviet geologists suggested that this area contains 

the largest concentration of lithium-bearing pegmatites in the world. In addition to lithium, these 

pegmatites are enriched in other rare metals such as tantalum, niobium, beryllium, tin, and cesium. 

Gem-quality tourmaline, kunzite, beryl, and optical grade quartz have been mined from some of these 

pegmatites. The pegmatites discussed in this report occur within the Nuristan rare-metal pegmatite area 

of interest (AOI).

Rare-metal pegmatites in the Nuristan rare-metal pegmatite AOI are found within Early 

Proterozoic and Late Triassic metamorphic rocks. These pegmatites are spatially and genetically related 

to Oligocene-age two-mica granites which represent the youngest of three phases of the Laghman

intrusive complex. The two-mica granites are regarded as fertile granites because the associated 

pegmatites are enriched in rare metals such as lithium, tantalum, niobium, beryllium, tin, and cesium. 

Two pegmatite belts—the Nuristan and Hindukush—flank the Alingar Pluton on the east and west sides, 

respectively. The central part of the Nuristan pegmatite belt lies within the Nuristan rare-metal 

pegmatite AOI, and identified rare-metal pegmatites are concentrated in four pegmatite fields: Pacigram, 

Paron, Kantiway, and Darrahe Pec. Geologic maps suggest that numerous unclassified pegmatites are 

present in much of the Nuristan pegmatite belt and suggest additional and unrecognized mineralization 

may be present.

Pegmatite districts in the Nuristan rare-metal pegmatite AOI exhibit vertical zonation from 

relatively barren pegmatites to those enriched in the rare metals. Many pegmatites are quite extensive 

with strike lengths on the order of 2 to 5 kilometers and widths ranging from 1 to 60 meters.

Exploration and assessment of these pegmatites for economic concentrations of rare metals may 

be facilitated by their size and probably excellent exposure in the mountainous terrain. However, access 

to this area is limited by the mountainous terrain and by a poor road and trail network.

24A.1 Introduction

This chapter summarizes and interprets results for the Nuristan rare-metal pegmatite area of 

interest (AOI) from geologic and compilation activities conducted during 2009 to 2011 by the 

U.S. Geological Survey (USGS), the U.S. Department of Defense Task Force for Business and Stability 

Operations (TFBSO), and the Afghanistan Geological Survey (AGS). Accompanying complementary 

chapters 24B and 24C address hyperspectral data and geohydrologic assessments, respectively, of the 

Nuristan rare-metal pegmatite AOI. Additional supporting data for this chapter are available from the 

Afghanistan Ministry of Mines in Kabul.

Pegmatites are one source for rare metals such as lithium, tantalum, niobium, beryllium, tin, and 

cesium, which are in demand for their individual properties or properties that they impart to other 

materials or metals (Kunaz, 1994; Harben and Kužvart, 1996). Although lithium-bearing brines have 

replaced lithium-bearing pegmatites as the principal source of lithium, current and future demand for 

lithium may result in a return to mining of lithium-bearing pegmatites. The pegmatites in northeastern 

Afghanistan are described as the largest concentration of lithium-bearing pegmatites in the world 
Chapter 24A. Summary for the Mineral Information Package for the Nuristan Rare-Metal Pegmatite Area of Interest 1631

(Rossovskiy and Chmyrev, 1977) and could be considered as the world’s recognized future principal 

source of lithium. The world’s supply of tantalum, niobium, and cesium comes from only a few large 

pegmatites, such as Tanco in Manitoba (Crouse and Černý, 1972; Stilling and Černý, 2006), 

Greenbushes in Western Australia (Partington, 1990; Partington and McNaughton, 1995; Harben and 

Kužvart, 1996), and Bikita in Zimbabwe (Harben and Kužvart, 1996). The Big Whopper Pegmatite in 

Ontario is a recently explored, large pegmatite of economic significance enriched in lithium, tantalum, 

cesium, and rubidium (Avalon, 2010). Although more than 90 percent of the world’s beryllium 

resources are in pegmatites, only about 40 percent of the beryllium production is from pegmatites 

(Harben and Kužvart, 1996). About 60 percent of the world’s beryllium production is from bertrandite 

replacement of altered rhyolite tuffs at Spor Mountain, Utah (Harben and Kužvart, 1996).

The Nuristan rare-metal pegmatite AOI lies in the Hindu Kush Mountains in northeastern 

Afghanistan, approximately 135 kilometers (km) northeast of Kabul (fig. 24A–1). The Nuristan 

rare-metal pegmatite AOI lies mainly within Nuristan and Kunar Provinces, with small portions in 

Badakshan and Lagham Provinces (fig. 24A–1). The main districts are Matal, Kamdesh, Kuran Wa 

Munjan, Wama, Waygal, Pech, Chapa Dara, and Nuristan. The Nuristan rare-metal pegmatite AOI 

covers an area of about 3.5 square kilometers (km2

) and includes four important pegmatite fields: 

Pacigram, Paron, Kantiway, and Darrahe Pec.

The names of pegmatites and pegmatite fields have various spellings in the literature; the 

principal spellings used in this summary are based on those shown by Rossovskiy and Nuiskov 

(1974a,b). It was not always possible to determine if names of features by different or the same authors 

were supposed to be the same, such as Paran, Paron, Parun, Parum, or different features.

24A.2 Previous Work

Pegmatites within the Nuristan rare-metal pegmatite AOI were poorly known to the western 

world until Soviet geologists began mapping the geology and assessing the mineral resources of 

northern Afghanistan in the 1960s and 1970s. Soviet geologists contributed an immense body of work 

on the pegmatites through geologic mapping, sampling, and interpretation (Narodnyi, 1965; Chmyriov 

and Mizrad, 1972; Cmyriov and others, 1973; Filippov, 1974; Rossovskiy, 1974, 1977, 1980, 1981a, b, 

1986, 1990; Rossovskiy and Nuiskov, 1974a, b; Rossovskiy and Chmyrev, 1976; 1977; Rossovskiy and 

Konovalenko, 1976, 1979, 1980; Rossovskiy and others, 1976a-e, 1977a, b, 1978 1979, 1987; Alemyar 

and others, 1977a, b; Bogatskiy and others, 1978; Rossovskiy and Shmakin, 1978; Shmakin and

Rossovskiy, 1978; Geruvol’ and others, 1980; Konovalenko and others, 1982; Vityaz and others, 1983; 

Fenogenov and Musazai, 1989). More recent studies have focused on those Afghanistan pegmatites that 

contain gem- or museum-quality mineral specimens (Bariand and Poullen, 1978; Bowersox and 

Chamberlain, 1995; Abdullah and Chmyriov, 2008).

The geology and mineral resources of Afghanistan have been summarized by Abdullah and 

others (1977), Orris and Bliss (2002), Doebrich and Wahl (2006), Peters and others (2007), and 

Abdullah and Chmyriov (2008). These publications contain more information regarding pegmatites in 

northeastern Afghanistan.

24A.3 Geology

The oldest rocks in the Nuristan rare-metal pegmatite AOI are Early Proterozoic metamorphic 

rocks that are divided into an Early Part, a Middle Part, and a Late Part (figs. 24A–2, 24A–3). Early Part 

rocks consist of mica, biotite, biotite-amphibole, garnet-biotite, garnet-sillimanite-biotite, and pyroxeneamphibole gneiss, as well as plagiogneiss, schist, migmatite, quartzite, marble, and amphibolite. Middle 

Part rocks consist of biotite and garnet-staurolite-biotite gneiss and schist, quartzite, marble, and 

amphibolite. Late Part rocks consist of biotite and garnet-biotite gneiss and schist, quartzite, marble, and 

amphibolite. Metamorphic grade of the Proterozoic rocks is either epidote-amphibolite or muscovitestaurolite-schist facies (Rossovskiy and Chmyrev, 1977). Younger lithologies include CarboniferousEarly Permian sandstone, siltstone, shale, and mafic-volcanic rocks and Late Triassic (Noria-Rhaetian) 
1632 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

siltstone, sandstone, shale, and conglomerate (Doebrich and Wahl, 2006). Descriptions of the individual 

pegmatite fields and deposits indicate that the Carboniferous-Early Permian and Late Triassic rocks 

have been metamorphosed (Abdullah and Chmyriov, 2008). 

Figure 24A–1. Index map showing the location of the Nuristan rare-metal pegmatite area of interest. Stars 

indicate major pegmatite deposits.
Chapter 24A. Summary for the Mineral Information Package for the Nuristan Rare-Metal Pegmatite Area of Interest 1633

The Nuristan rare-metal pegmatite AOI and surrounding areas are characterized by northeasttrending structures and similar trending belts of rocks. The belts are composed of Early Proterozoic, 

Carboniferous to Early Permian, and Late Triassic rocks, which are bounded by northeast-trending faults 

(figs. 24A–2, 24A–3). Oligocene-age granite intrusions are also elongate along the same structural 

trends. Neither rock type nor the faults appear to have a great effect on the topography. 

A narrow, northeast-trending, elongate structural block of Carboniferous to Early Permian 

sandstone, siltstone, shale, and mafic volcanic rocks is fault bounded on the east and west, and bordered 

by Early Proterozoic (Early Part) metamorphic rocks (figs. 24A–2, 24A–3). A number of 

northeast-trending, elongate, Oligocene-age granites are located along and on either side of these 

boundary faults (fig. 24A–4).

A much larger block of Late Triassic rocks extends nearly the entire length of the Nuristan 

rare-metal pegmatite AOI and is fault bounded with Early Proterozoic (Early Part) metamorphic rocks 

on the west and by Early Proterozoic (Early Part and Late Part) metamorphic rocks on the east 

(figs. 24A–2, 24A–3) . As with the Carboniferous-Early Permian block, Oligocene-age granite 

intrusions are elongate within and outside of the Triassic fault block with some of the intrusions 

appearing to cross the faults. Strike symbols depicted on the map of Doebrich and Wahl (2006) are 

oriented approximately along the same structural trends.

24A.3.1 Oligocene and Older Intrusions

The Early Cretaceous age Nilau igneous complex (K1gbm) at the southern end of the Nuristan 

rare-metal pegmatite AOI (figs. 24A–2, 24A–3) is composed of gabbro, monzonite, diorite and 

granodiorite. It intrudes rocks of Early Proterozoic age and Triassic age. Major northeast-trending faults 

cut and offset portions of this complex. The Darrahe Pec pegmatite field is located mainly within this 

complex.

The rare-metal pegmatites are genetically and spatially related to the Oligocene-age granitic 

intrusions, and these granites are described below. Granitoid intrusive rocks in northeastern Afghanistan 

are widespread (figs. 24A–2, 24A–3) and form large, northeast-oriented massifs. These massifs are 

localized within a sequence of Proterozoic and Carboniferous gneisses and schists and Triassic clastic 

sedimentary rocks. The largest granitoid massif is the Oligocene-age Laghman intrusive complex, which 

is located in the Nuristan Fault Block (Abdullah and Chmyriov, 2008). The Nuristan Fault Block and the 

Laghman intrusive complex are not depicted on any map inspected for northeastern Afghanistan. This 

fault block may lie between the Mississippian rocks (fig. 24A–2) located to the northwest and southeast. 

The Laghman intrusive complex is separated into three main phases. Phase I rocks of the 

Laghman intrusive complex include diorite, quartz diorite, granodiorite, tonalite, granosyenite, and 

plagiogranite (Abdullah and Chmyriov, 2008). Phase II rocks include medium- and coarse-grained, 

commonly porphyritic biotite and amphibole-biotite granite and granodiorite (Rossovskiy and Chmyrev, 

1977; Abdullah and Chmyriov, 2008). Phase III rocks include biotite and two-mica granite, granite 

porphyry, and aplitic and pegmatoid granite (Rossovskiy and Chmyrev, 1977; Abdullah and Chmyriov, 

2008). Rare-metal pegmatites are spatially and probably genetically related to Phase III granites and 

intrude the earlier Laghman intrusive complex phases. 

The Alingar Pluton is described as a massif of the Laghman intrusive complex, but the literature 

is unclear about the spatial distributions of the Laghman intrusive complex and the Alingar Pluton 

(Rossovskiy and Chmyrev, 1977), and no map showing the outlines or any location of these units was 

found. Based on the references to these igneous units, most of the Alingar Pluton lies between the 

Hindukush and Nuristan pegmatite belts (fig. 24A–2), and the Laghman intrusive complex includes both 

the Alingar Pluton in figure 24A–2 and the rest of the Oligocene intrusive rocks in the western part of 

figure 24A–2. Given that Alingar Pluton is part of the Laghman intrusive complex, it likely have the 

same phases as the larger unit. Most of the exposed portion of this pluton lies west of the Nuristan 

rare-metal pegmatite AOI (fig. 24A–2). 
1634 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

Figure 24A–2. Regional geologic map showing the major granitic bodies of the Pagram intrusive complex, faults, 

and pegmatite belts, fields, and the Nuristan rare-metal pegmatite area of interest. Units from Doebrich and Wahl 

(2006).
Chapter 24A. Summary for the Mineral Information Package for the Nuristan Rare-Metal Pegmatite Area of Interest 1635

Figure 24A–3. Geologic map of the Nuristan rare-metal pegmatite area of interest with pegmatite belts, fields, 

and deposits. Units from Doebrich and Wahl (2006).

Figure 24A–4. Diagrammatic geologic cross section of the Paron graben-syncline (modified from Rossovskiy and 

Konovalenko, 1979). (Many maps and diagrams in the Russian literature lack vertical and horizontal scales.)
1636 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

The biotite and two-mica granites are light-gray or gray and fine- and medium-grained. The 

composition of the granites is 30 to 50 volume percent potassium feldspar, 25 to 30 volume percent 

quartz, 20 volume percent albite-oligoclase, and 5 to 10 percent biotite and muscovite (Rossovskiy and 

Chmyrev, 1977). The average composition of 12 samples of two-mica granites from Phase III of the 

Laghman complex is 71.97 weight percent SiO2, 0.40 weight percent TiO2, 14.33 weight percent Al2O3, 

0.14 weight percent FeO, 2.01 weight percent MnO, 0.06 weight percent MgO, 0.87 weight percent 

CaO, 3.37 weight percent Na2O, 4.09 weight percent K2O, 0.17 weight percent P2O5, and 0.47 weight 

percent calculated loss (based on data from Rossovskiy and Chmyrev, 1977).

Phase III granites are generally small, with dimensions on the order of 1 to 5 km up to5 to 30 km. 

These intrusions are commonly elongated layer-like bodies that are conformable with the strike of the 

surrounding rocks and are commonly located along major northeasterly striking faults. They also 

commonly occur in the contact zones between the gneiss sequences of the Nuristan series and Upper 

Triassic rocks (Rossovskiy and Chmyrev, 1977).

The two-mica granite and pegmatite intrusions are guided mainly by the structural characteristics 

of the host rocks rather than by the host rock composition (Rossovskiy and Chmyrev, 1977). Most of the 

rare-metal pegmatites are intruded into quartz-muscovite-biotite schists with garnet and staurolite. These 

pegmatites are also found in gabbro-diorites, diorites, gneisses, limestones, and amphibolites, but to a 

much lesser extent.

Phase II granites of the Oligocene-age Alingar Pluton are bounded by the fault on the western 

side of the Triassic fault block. Phase I granites of the same intrusive complex are, in some cases cut by 

the faults, and in others, they apparently are guided by the faults and some may cross the faults. This 

suggests that some fault movement occurred subsequent to formation of the Phase II granites, and 

perhaps during and after the Phase I granites.

24A.3.2 Metallogeny

The Nuristan and Hindukush pegmatite belts belong to a Himalayan pegmatite megabelt that 

extends from northeastern Afghanistan through Pakistan and into India, Nepal, and Bhutan (Baratov and 

Rossovskiy, 1987). Throughout this megabelt, rare-metal pegmatites are associated with two-mica, 

peraluminous granite batholiths. In addition to rare-metal pegmatites, gem-quality kunzite (a pink to 

violet, clear spodumene), tourmaline, aquamarine, morganite, emeralds, and sapphires are found in 

association with some of these pegmatites. These pegmatites are also sources for museum-quality 

mineral specimens (Baratov and Rossovskiy, 1986; Bariand and Poullen, 1978; Bowersox and 

Chamberlain, 1995).

The metallogenic specificity of rare-metal pegmatite belts may be dependent on (1) the overall 

geochemistry of the province, (2) the composition of the fertile granites within different tectonic zones, 

(3) the tectonic regime during emplacement of the pegmatites, and (4) the structure and morphology of 

the pegmatite veins (Rossovskiy, 1990, 1991). Overall, the pegmatites of the Pamir-Hindu Kush 

pegmatite province (Rossovskiy and Mogarovskiy, 1988), which includes the Hindukush and Nurestan 

pegmatite belts (fig. 24A–2), are anomalous in lithium, beryllium, tantalum, and tin ,with a general 

enrichment of cesium in the Hindukush region (Rossovskiy, 1990, 1991). As the granites are S-type 

granites, this suggests that the sediments from which these granites were derived were anomalous in 

these elements (Rossovskiy and Mogarovskiy, 1988). The enrichment of lithium, rubidium, and cesium 

in pegmatitic fluids may result from conversion of biotite to muscovite in the two-mica granites at the 

end of granite crystallization (Rossovskiy and Mogarovskiy, 1988).

Pegmatites can be classified using petrogenetic criteria based on how pegmatites develop by 

igneous differentiation from various plutonic source magmas (Černý and Ercit, 2005). For example, the 

NYF family of pegmatites exhibits a progressive accumulation of niobium, yttrium, and fluorine along 

with beryllium, rare-earth elements (REE), scandium, titanium, zirconium, thorium, and uranium. The 

NYF family of pegmatites results from fractionation of subaluminous to metaluminous A- and I-type 

granites. The A- and I-type granites may be derived from depleted crust or mantle contributions. This 
Chapter 24A. Summary for the Mineral Information Package for the Nuristan Rare-Metal Pegmatite Area of Interest 1637

can be compared to the LCT family of pegmatites, which exhibits an accumulation of lithium, niobium, 

cesium, and tantalum along with rubidium, beryllium, tin, boron, phosphorous, and fluorine. These are 

derived mainly from peraluminous S-type granites, and less commonly from I-type granites (Černý and 

Ercit, 2005). The pegmatites in the Nuristan rare-metal pegmatite AOI belong primarily to the LCT 

family.

24A.4 Economic Geology

24A.4.1 Pegmatite Provinces, Belts, Fields, and Groups

Pegmatite provinces are defined by the total pegmatite fields (or belts) within metallogenic 

provinces (Černý, 1982a). Pegmatite belts consist of pegmatite fields, which are related to large-scale 

linear structures such as lineaments, deep faults, or margins of granite plutons (Černý, 1982a). Two 

major pegmatite belts are associated with the Alingar Pluton. The Nuristan pegmatite belt lies along the 

eastern flank of the pluton, and the Hindukush belt lies along the western flank (figs. 24A–2, 24A–3). 

Each belt consists of several pegmatite fields, which, in turn contain one or more named pegmatites and 

probably numerous unnamed pegmatites. 

Pegmatite fields are areas that contain related pegmatites in a common geological-structural 

environment, and with a common age and igneous source (Černý, 1982a). The Hindukush belt consists 

of the Mundol, Nilaw-Kolum, Nilaw, Alingar, Samakat, and Sahidan pegmatite fields. The Nuristan 

pegmatite belt consists of the Iska-Sem, Pacigram, Paran (Jamanak-Pasghushta), Kantiway, Darrahe 

Pec, Cawgao, Surkhrud, and Darrah Nur pegmatite fields (Rossovskiy and Nuiskov, 1974b) and extends 

beyond the northern and southern boundaries of the Nuristan rare-metal pegmatite AOI. The Iska-Sem, 

Cawgao, Surkhrud, and Darrah Nur pegmatite fields of the Nuristan pegmatite belt also lie outside of the 

Nuristan pegmatite belt. A summary of the pegmatite fields that lie mostly within the Nuristan 

rare-metal pegmatite AOI is presented in table 24A–1. The reporting of the presence of economic 

minerals is no guarantee a viable deposit is present without subsequence evaluation identifying grade, 

size, and other factors.

Table 24A–1. Pegmatite fields and their reported economic minerals in the Nuristan rare-metal pegmatite area of 

interest. [Be, beryllium; Cs, cesium; ESCAP, United Nations Economic and Social Commission for Asia and the Pacific; Li, lithium; 

Nb, niobium; Rb, rubidium; Sn, tin; Ta, tantalum] 

Locality/deposit 

name

Province

Approximate 

size (square 

kilometers) 

Commodities

Significant minerals or 

materials (other than 

quartz, mica, feldspar)

Selected references

Paron (JamanakPasgushta) 

Pacigram 

(Pachigram) 

Darrahe Pec 

(Darra-i-Pech) 

Kantiway 

Nuristan

Nuristan 

Kunar

Nuristan

1,158

221

85

130

Li, Ta, Nb, Sn,

Cs, Rb

Li, Be, Sn, Nb 

Be, Nb, Ta, Li, 

mica

gemstones, Li,

quartz

columbite, cassiterite, 

schorl, garnet, beryl

spodumene, schorl 

spodumene, tantalite,

spodumene, beryl, 

columbite-tantalite, 

pollucite

kunzite, spodumene, 

tourmaline, cassiterite, 

cleavelandite,

ESCAP, 1995; Abdullah and 

Chmyriov, 2008

ESCAP, 1995; Abdullah and 

Chmyriov, 2008

ESCAP, 1995; Rossovskiy,

1977; Abdullah and 

Chmyriov, 2008

ESCAP, 1995; Abdullah and 

Chmyriov, 2008

Locations of pegmatite fields, deposits, and individual pegmatites were derived by rectifying and 

digitizing locations shown on a map by Rossovskiy and Nuiskov (1974a,b). Because of the scale of the 

original map, some uncertainty as to exact locations of these features is to be expected. A summary of 

the named pegmatites, their locations, approximate elevations, and their mineralogy is presented in 

table 24A–2. 

Pegmatite groups include a local group of closely spaced pegmatites of a single type, with a 

common geological-structural position within a pegmatite field (Černý, 1982a). Although pegmatite 
1638 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

groups in the Nuristan rare-metal pegmatite AOI are not generally referred to as pegmatite groups, 

descriptions of pegmatite deposits suggest that many of these can be referred to as pegmatite groups. 

Table 24A–2. Pegmatites, pegmatite fields, locations, and significant minerals. 

[Data are from United Nations Economic and Social Commission for Asia and the Pacific

Chmyriov (2008). Al, aluminum; Ca, calcium; Ta, tantalum]

(1995) and Abdullah and 

Pegmatite name Pegmatite field East 

longitude

North 

latitude

Elevation 

above sea

level 

(meters) 

Mineralogy

Paprok (Papruk)

Pakavaipet 

(Pakawalpet)

Alma

Jamanak

Pasgusta 

(Pasghushta) 

Pasgusta-under 

(Pasghushta 

Lower)

Pramgal

Drumgal

Paski (Pashki)

Tsamgal 

(Tsamghal)

Camgal (Zamgal)

Insahar 

(Inshaghar)

Boni (Bori)

Aramc (Aranch)

Nangalam

Wasgul (Wozgul)

Yorigul (Yorigal, 

Yarigul)

Kantiway

Dara-i-Pech

Paron (JamanakPasghushta)

Paron (JamanakPasghushta)

Paron (JamanakPasghushta)

Paron (JamanakPasghushta)

Paron (JamanakPasghushta)

Paron (JamanakPasghushta)

Paron (JamanakPasghushta)

Paron (JamanakPasghushta)

Paron (JamanakPasghushta)

Paron (JamanakPasghushta)

Paron (JamanakPasghushta)

Paron (JamanakPasghushta)

Paron (JamanakPasghushta)

Paron (JamanakPasghushta)

Paron (JamanakPasghushta)

Paron (JamanakPasghushta) 

Paron (JamanakPasghushta)

Kantiway

Dara-i-Pech

71.1501

71.1245

71.1872

70.9798

71.002

71.021

71.0852

71.0093

70.9507

71.0419

71.0444

70.9948

70.8401

70.9650 

70.8872

70.9956

70.8665

70.7346

70.6167

35.5987

35.5757

35.5090

35.3707

35.38

35.369

35.3663

35.3190

35.3031

35.2958

35.3012

35.2403

35.1830

35.1438

34.9915

35.4771

35.3624

35.2941

34.9998

4,060

3,450

3,980

3,770

4,680

4,470

3,500

3,450

3,800

3,140

3,080

2,245

2,660

2,370

1,360

3,920

4,190

3,480

2,596

Spodumene, lepidolite, albite, microcline, 

polychromic tourmaline, columbite-tantalite,

cassiterite

Spodumene, lepidolite, albite, microcline, 

polychromic tourmaline, columbite-tantalite, 

cassiterite

Spodumene, lepidolite, albite, microcline, beryl, 

polychromic tourmaline, columbite-tantalite, 

cassiterite

Spodumene, cirnolite (may be cirrolite, a Ca-Al 

phosphate)

Spodumene, columbite-tantalite, cassiterite

Spodumene, muscovite, cleavelandite

Spodumene, lepidolite, albite, microcline, 

polychromic tourmaline, columbite-tantalite, 

cassiterite

Spodumene

Spodumene, pollucite

Spodumene

Spodumene

Spodumene, lepidolite, albite, microcline, 

polychromic tourmaline, columbite-tantalite, 

cassiterite

Spodumene, lepidolite, albite, microcline, 

polychromic tourmaline, columbite-tantalite, 

cassiterite

Spodumene, lepidolite, albite, microcline, beryl, 

polychromic tourmaline, columbite-tantalite, 

cassiterite

Spodumene, rubellite

Spodumene, lepidolite, albite, microcline, 

polychromic tourmaline, columbite-tantalite, 

cassiterite

Prospective for Ta

Spodumene, lepidolite, albite, microcline, 

polychromic tourmaline, columbite-tantalite, 

cassiterite, kunzite, quartz crystal

beryl
Chapter 24A. Summary for the Mineral Information Package for the Nuristan Rare-Metal Pegmatite Area of Interest 1639

Pegmatite name Pegmatite field East 

longitude

North 

latitude

Elevation 

above sea

level 

(meters)

Mineralogy

Dara-i-Pech 

(Vora Des)

Dara-i-Pech 70.7413 34.9276 2,100 beryl, columbite-tantalite, spodumene

Gursaisk 

(Ghursalak)

Dara-i-Pech 70.7259

(70.7389)

34.9644

(34.9631)

1,495 beryl, columbite-tantalite, cassiterite

Awlaghal Dara-i-Pech 70.7234 34.9434 1,914 Spodumene, cassiterite, beryl, schorl

Darrahe Dara-i-Pech 70.7201 34.8976 2,680 Beryl, pollucite

Paciram 

(Pachigram)

Pachigram 71.1762 35.7682 4,170 Spodumene, lepidolite, albite, microcline, 

polychromic tourmaline, columbite-tantalite, 

cassiterite

Tsamgal Pachigram 71.0419 35.2958 3,145 Spodumene

Canigal Pachigram 71.1184 35.7278 3,690 Spodumene

Dega (Degha) Pachigram 71.0641 35.6381 4,270 Spodumene, lepidolite, albite, microcline, 

polychromic tourmaline, columbite-tantalite

Tsotsum Pachigram 71 35.5833 3,945 Tourmaline

Mualevi Pachigram 71.0832 35.7667 4,702 Tourmaline

24A.4.2 Pegmatite Fields

24A.4.2.1 Paron (Jamanak-Pasghushta) Pegmatite Field

The Paron (Jamanak-Pasghushta) pegmatite field (figs. 24A–2, 24A–3) is situated in the 

north-east of the Nuristan Province in Early Proterozoic metamorphic schists, as well as in slightly 

metamorphosed sedimentary rocks of Late Triassic age (Abdullah and Chmyriov, 2008). The Paron field 

pegmatites were intruded adjacent to an Oligocene granite intrusion. The Paron field is important 

primarily for lithium, which occurs here in the lithium-bearing pyroxene, spodumene. This field contains 

two long zones (groups) of spodumene dikes, the Paprok and Waygal, and two shorter zones (groups), 

the Pasgusta and Drumgal. In the Paprok zone, spodumene dikes have been defined at Pakawalpet, 

Jamanak, Pashki, and Boni.. In the Waygal zone, spodumene dikes have been defined at Alma, Tramgal, 

Samgal, Inshaghar, Aranch, and Nangalam. Five large lithium deposits are included in this field: 

Jamapak, Pasgusta, Drumgal, Canga, and Pasghushta Lower. Veins and vein zones of the spodumenealbite pegmatites are up to 1 to 5 km in length and 20 to 40 m wide (Abdullah and Chmyriov, 2008). 

The types of pegmatites in this field include:

1. oligoclase-microcline biotite-muscovite (barren); 

2. schorl-muscovite-microcline with beryl;

3. albitized microcline and albite with lithium phosphate;

4. spodumene-microcline-albite and spodumene-albite; and

5. spodumene-microcline cleavelandite with pollucite and tantalite (Abdullah and Chmyriov, 

2008). 

24A.4.2.2 Pacigram (Pachigram) Pegmatite Field

The Pacigram pegmatite field is confined to a narrow and long graben syncline (a term used by 

Adullah and Chyriov, 2008) that appears to indicate a graben containing rocks folded into a synclinal 

structure) involving Upper Carboniferous to Lower Permian schist and Proterozoic schist and gneiss that 

are intruded by Oligocene granite (figs. 24A–2, 24A–3). Three types of pegmatite dikes have been 

distinguished in the area: 

1. oligoclase-microcline, schorl tourmaline-muscovite; 

2. albite with much phosphate; and 

3. spodumene-microcline-albite and spodumene-albite (Abdullah and Chmyriov, 2008). 

The spodumene-microcline-albite and spodumene-albite pegmatites may be economic and are 

found at Dega, Canigal, and Pachigram. At least 100 pegmatite dikes are currently known. Thickness of 

the pegmatites ranges from 1 to 20 m wide, and they are 10 m to 1 km in length. Pegmatite samples can 
1640 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

have 0.3 to 5 weight percent Li2O, 0.001 to 0.01 weight percent Nb2O5, 0.001 to 0.01 weight percent 

BeO, and 0.006 to 0.04 weight percent Sn (Abdullah and Chmyriov, 2008). 

24A.4.2.2.1 Pasgusta (Pashgushta) Deposit

The Pasgusta deposit (figs. 24.0A–2, 24A–3) contains a zone of steeply dipping pegmatite dikes 

in Upper Triassic schist. This zone varies in width between 30 and 250 m and extends for about 10 km. 

The largest dikes are up to 600 to 800 m long and 20 to 30 m wide. The pegmatites are of the 

spodumene-microcline-albite and spodumene-albite types and contain finely disseminated columbitetantalite minerals and some cassiterite. Three spodumene dikes in the upper reaches of the Pasgushta 

River total 70 m in thickness and contain an average Li2O content of 1.96 weight percent. In the area of 

Pasgushta Pass, a 20-m interval contains an average Li2O content of 2.14 weight percent. Speculative 

Li2O reserves of the Pashgushta deposit are 1,050,000 tonnes (t) to a depth of 100 m. The Rb and Cs 

content is less than a few hundredths of 1 percent. The Ta2O5 content varies between 0.002 and 0.007 

weight percent (Abdullah and Chmyriov, 2008). 

24A.4.2.2.2 Drumgal Deposit

The Drumgal pegmatite bodies were intruded into Upper Triassic schist (figs. 24A–2, 24A–3). 

The three spodumene-microcline-albite pegmatite dikes that currently comprise this deposit vary in 

thickness from 7 to 30 m and are between 1 and 2 km in length. The Li2O content ranges from 1.38 to 

1.58 weight percent. Speculative Li2O reserves were calculated to be 253,000 t to a depth of 100 m. In 

one pegmatite dike, a 30-m interval contains 0.06 weight percent Ta2O5 with a tantalum to niobium ratio

of less than 5:1. The Ta2O5 content averages 0.03 weight percent over the full 60 m thickness of the dike 

(Abdullah and Chmyriov, 2008). 

24A.4.2.2.3 Jamanak Deposit

Pegmatites in the main part of the deposit were emplaced in Triassic age quartz-muscovitebiotite, garnet-staurolite-mica, and biotite schists over an area of about 2 km2 (figs. 24A–2, 24A–3).

Three types of pegmatite dikes are recognized:

1. spodumene-microcline-albite;

2. strongly albitized pegmatite with spodumene and cymatolite (a mixture of albite and muscovite 

usually replacing spodumene); and 

3. albite (Abdullah and Chmyriov, 2008). 

At the Jamanak deposit, the spodumene dikes make up four zones or groups. Those of the first 

zone range in width from 10 to 20 m and extend as far as 1 km, being composed of the following 

mineral assemblage:

1. 60 to 65 percent spodumene-microcline-albite;

2. 15 percent spodumene-microcline-quartz;

3. 15 to 20 percent spodumene-albite; and

4. 5 to 10 percent albite (Abdullah and Chmyriov, 2008). 

The second zone ranges from 10 to 15 m thick; the third, 5 to 7 m thick, and the fourth, 2 to 6 m 

thick. The lengths of both the second and fourth pegmatite zones are 800 m, while the third zone 

exceeds 2 km in length. The Rb and Cs content of the pegmatite zones is 0.02 weight percent or less and 

the Ta2O5 content is 0.006 weight percent. The average Li2O content of the deposit is 1.53 weight 

percent. The speculative Li2O reserves to a depth of 100 to 250 m total 294,000 t for zones I, II, and III. 

The total Li2O reserves of the entire deposit to a depth of 100 m are 450,000 t (Abdullah and Chmyriov, 

2008). 

24A.4.2.2.4 Yorigal (Yarigul) Deposit

The pegmatites of the Yorigal deposit occur in Proterozoic schist and gneiss (figs. 24A–2, 

24A–3) and contain large crystals of muscovite, schorl, and beryl. The thickness of the pegmatite dikes 

ranges from 1.5 to 5.0 m, and the lengths are from 0.5 to 3.5 km. Pegmatite dikes are of the 
Chapter 24A. Summary for the Mineral Information Package for the Nuristan Rare-Metal Pegmatite Area of Interest 1641

spodumene microcline-albite type. The speculative lithium oxide reserves are 130,000 t. The almost 

flat-lying dikes of the Yorigal deposit are similar to dikes in the Wasgul area, and may be 

tantalum-bearing (Abdullah and Chmyriov, 2008). 

24A.4.2.2.5 Pasgusta-Under (Lower Pasgushta) Deposit

The Pasgusta-under deposit consists of two tabular pegmatite dikes in Upper Triassic schist 

(figs. 24A–2, 24A–3). Their thickness ranges from 20 to 25 m, and lengths are 500 and 750 m. The 

pegmatite, which is of the spodumene-albite type, has the following mineral composition: 10 to 

15 volume percent microcline blocks, 25 to 30 percent spodumene crystals, 60 volume percent 

fine-grained muscovite-quartz-albite aggregates, and 1 to 3 volume percent other mineral aggregates 

(cleavelandite). The Li2O is uniformly distributed within the dikes, with the content in the range from 

2.00 to 2.31 weight percent (2.2 percent on the average). Possible Li2O reserves to a depth of 100 m are 

124,000 t (Abdullah and Chmyriov, 2008). 

24A.4.2.2.6 Pashki Deposit

Pegmatites in the Pashki deposit were intruded into metamorphosed Upper Triassic sedimentary 

rocks (figs. 24A–2, 24A–3). Four types of pegmatite have been recognized within an area of 

approximately 7 km2

: 

1. albitized microcline with densely disseminated phosphate minerals and scarce beryl;

2. spodumene microcline-albite;

3. heavily albitized, with spodumene; and 

4. spodumene-cleavelandite microcline with pollucite (Abdullah and Chmyriov, 2008). 

The principal types of ore-bearing pegmatites are those that contain spodumene, microcline, and 

albite. Two large dikes, Dikes 1 and 3, and Dike Zone 2 are of this type. Dike 1 is 1 km in length and 

ranges in thickness from 7.5 to 60 m. Dike 1 is exposed for 600 m down dip by erosion and contains 15 

to 25 volume percent spodumene. Dike 3 is 600 m in length and 2 to 8 m in thickness. This dike 

contains 15 to 20 volume percent spodumene. Pegmatite dikes in Dike Zone 2 vary in thickness between 

0.5 and 10 m and have a total thickness of 5 to 10 m. While Dike Zone 2 may extend for a distance of 

2.5 km, individual pegmatite dikes may range from 5 to 300 m. In some places, the spodumene dikes are 

arranged en echelon, and in other places they form a complex network of subparallel dikes. The dikes 

contain between 0.01 and 0.02 weight percent Rb and Cs and between 0.002 and 0.008 weight percent 

Ta2O5. Dike 1 contains an average of 1.46 weight percent Li2O; Dike 3 contains an average of 

1.56 weight percent Li2O. Pegmatites in Dike Zone 2 contain an average of 2.1 weight percent Li2O. 

Total possible Li2O reserves of Dikes 1 and 3 and dikes in Zone 2 to a depth of 100 m are 127,000 t 

(Abdullah and Chmyriov, 2008). 

24A.4.2.3 Darrahe Pec Pegmatite Field

The Darrahe Pec pegmatite field is located mainly within the Early Cretaceous age Nilau igneous 

complex at the southern end of the Nuristan rare-metal pegmatite AOI (figs. 24A–2, 24A–3). The 

pegmatites are emplaced in gabbro and diorite. This is a rather small field, on the order of 85 km2. The 

Darrahe Pec pegmatite field contains the following types of pegmatites:

1. oligoclase-microcline, schorl tourmaline-biotite-muscovite (barren) pegmatite;

2. albitized microcline pegmatite with coarse beryl; and

3. spodumene-microcline-albite pegmatite.

Albite-bearing pegmatites contain beryl and disseminated columbite-tantalite. The field includes 

the Darrhe-Pec deposit, which contains economic concentrations of lithium, beryllium, tantalum, 

tourmaline, and kunzite. 
1642 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

24A.4.2.4 Kantiway Pegmatite Field

The Kantiway pegmatite field is located within Proterozoic metamorphic rocks (figs. 24A–2, 

24A–3). This field is on the order of 130 km2 in area. This field contains four types of pegmatites which 

are similar to those from the Darrahe Pech:

1. oligoclase-microcline, schorl tourmaline-muscovite (barren); 

2. albitized microcline;

3. albite; and

4. spodumene-albite.

Some of the large spodumene-albite pegmatite dikes are rich in tantalite, kunzite, piezooptic (a 

change in refractive index induced by a change in pressure) quartz, and tourmaline. One pegmatite dike 

which was examined in detail was on the order of 300 m long and 0.5 to 15 m thick (Abdullah and 

Chmyriov, 2008). One 150-m2 section, containing cleavelandite aggregates with tourmaline and 

muscovite, was found to have cavities lined with smoky quartz, green tourmaline, and kunzite crystals. 

Cassiterite grains and manganotantalite lamellae are also present in that pegmatite (Abdullah and 

Chmyriov, 2008). 

24A.5 Vertical Zonation and Structural Patterns of Pegmatites Within Pegmatite 

Fields

Pegmatites within many pegmatite fields exhibit a pattern of vertical zonation that is also a 

common characteristic of pegmatites throughout the Nuristan rare-metal pegmatite AOI. In addition, 

pegmatite orientations are peculiar to some pegmatite fields and are most likely determined by the 

dominant host rock of that field. 

Fenogenov and Musazai (1989) documented a zonation in pegmatites over a vertical range of 

1,500 to 2,000 m in the Darrahe Pec and Drumgal deposits (figs. 24A–5, 24A–6, 24A–7. From top to 

bottom that zonation is described as: 

1. albite-spodumene with a large amount of microcline and a small admixture of cassiterite, beryl, 

and columbite; 

2. essentially albitic with rare spodumene, small phenocrysts beryl and tantalite-columbite; 

3. microcline-albitic with ore, screened beryl, and tantalite-columbite; and

4. essentially microcline with rare beryl.

A similar zonation was noted in the Nilau-Kulam field (Rossovskiy, 1981a, b) (figs. 24A–2, 

24A–8). From top to bottom that zonation is described as: 

1. lepidolite-spodumene-albite pegmatites; 

2. albite pegmatites with spodumene, polychrome tourmaline, and lepidolite; 

3. albitized microcline pegmatites with kunzite and vorobievite (this does not appear to be a valid 

mineral species); and

4. plagioclase-microcline and albitized microcline pegmatites with schorl and beryl.

The vertical zonation suggests differentiation of pegmatites from oligoclase-microcline-biotitemuscovite to lepidolite-spodumene-albite. This zonation pattern has important implications during the 

exploration of minerals of economic importance in a pegmatite field. If only the feldspar plus mica 

(barren) pegmatites are present, the upper pegmatites with minerals of importance have probably been 

removed by erosion. 

Vertical zonation from a two-mica granite to muscovite-feldspar pegmatites to beryl pegmatites 

and to lithium-rich pegmatites is a well documented fractionation trend in granitic magmas (Vlasov, 

1961; Černý, 1982a; London, 2008). Increased albitization accompanies increased fractionation in these 

pegmatites (fig. 24A–8).

In zoned districts the generalized sequence of pegmatites is (Černý, 1982a): 

1. barren pegmatites of granitic texture, with magnetite and biotite;

2. barren plagioclase-microcline pegmatites, partly graphic, with biotite and schorl;

3. microcline pegmatites, partly graphic, with schorl, muscovite, and beryl; 
Chapter 24A. Summary for the Mineral Information Package for the Nuristan Rare-Metal Pegmatite Area of Interest 1643

4. zoned microcline-albite pegmatites, partly albitized, with muscovite, schorl, beryl and Nb-Ta 

minerals;

5. zoned microcline-albite pegmatites, extensively replaced, with lithium, rubidium, cesium, 

tantalum, boron, phosphorous, and fluorine mineralization;

6. albite pegmatites with lithium, beryllium, tin, and tantalum mineralization;

7. relatively homogeneous albite-spodumene pegmatites with minor beryllium, tin, and tantalum 

mineralization;

8. essentially quartz veins with minor feldspar(s) and one or more of beryl, cassiterite, or 

wolframite.

The structural disposition of the pegmatites in various pegmatite fields is determined by either 

the host rock lithology or by the structural history of the host rocks, or both. Pegmatites are 

characterized as (1) steeply dipping veins, (2) flat to gently dipping sills, and (3) small intraformational 

lenticular bodies. Gently dipping pegmatite sills, which are characteristic of the Nilaw, Kulam, Darrahe 

Pech and some other fields, are developed mainly in gabbroic and diorite bodies of the Nilaw complex 

(figs. 24A–5, 24A–6, 24A–9, 24A–10). Some gently dipping and cross-cutting sills occur in Proterozoic 

gneiss in the Paran pegmatite field, also. Steeply dipping pegmatite veins in the Paran pegmatite field 

occur in schists and form linearly elongated zones which are conformable with the schistosity and fold 

patterns of the enclosing rocks (figs. 24A–10). Small intraformational lenticular bodies are associated 

with the contact zones of the Alingar Pluton. 

Steeply dipping veins appear to contain most of the important lithium deposits and occurrences. 

The gentle to flat-lying pegmatites contain important concentrations of beryllium, tantalum, precious 

stones, piezo-quartz, and tourmaline. Those pegmatites closely associated with the granites are 

commonly considered to be likely non-economic (Abdullah and Chmyriov, 2008). 

24A.6 Gemstone-Bearing Pegmatites

Relatively little is known about the potential of gemstone-bearing pegmatites in the Nuristan 

rare-metal pegmatite AOI. There is brief mention of gemstone-bearing pegmatites in the Kantiway 

pegmatite field. This field contains transparent crystals of green tourmaline and cassiterite grains, 

kunzite crystals, and manganotantalite lamellae (Abdullah and Chmyriov, 2008). Pegmatites in the 

Dara-i-Pech pegmatite field contain kunzite, and, as such, may also contain gem-quality tourmaline and 

beryl.

The more important and better known of the gemstone-bearing pegmatites in Afghanistan are in 

the Nilaw-Kulam pegmatite field (figs. 24A–2, 24A–3) which contain the Nilaw and Kulam deposits 

(Bariand, and Poullen, 1978; Bowersox and Chamberlain, 1995; Abdullah and Chmyriov, 2008). The 

Nilaw deposit consists of: 

1. albitized microcline pegmatite with hand-sorted coarse-crystalline beryl;

2. albite pegmatite carrying tantalum mineralization; and

3. lepidolite-spodumene-albite pegmatite with tantalum mineralization, piezooptic tourmaline, and 

kunzite mineralization.

The Kulam deposit consists of a gigantic vein of albitized microcline pegmatite bearing kunzite, 

rock crystal, aquamarine, tourmaline, coarse-crystalline beryl, tantalite, and pollucite (Abdullah and 

Chmyriov, 2008). 

24A.7 Estimation of Ore Reserves and Resources

In the Nuristan rare-metal pegmatite AOI, a number of economically viable pegmatites or 

pegmatite deposits, which may include one or more pegmatites, were proposed by Soviet geologists and 

noted in the succeeding literature (Abdullah and Chmyriov, 2008). The Pasgusta, Pasgusta-under, 

Camgal, Jamanak, and Drumgal deposits in the Paran pegmatite field (fig. 24A–3) are five large lithium 

deposits that also may contain economic concentrations of tantalum. The Darrahe Pec pegmatite field 

contains the Darrahe Pec deposit with potentially economic concentrations of lithium, beryllium, and 
1644 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

tantalum. Lepidolite, amblygonite, pollucite, and petalite are noted in the Hindukush Alingar and 

Samakat pegmatite fields in the Hindukush pegmatite belt and in the Paran field in the Nurestan 

pegmatite belt (fig. 24A–2).

Figure 24A–5. Map of pegmatite zoning at Darrahe Pec (Darai-Pich) deposit (modified from Fenogenov and 

Musazai, 1989). Section A-B is shown in figure 24A-6.

Table 24A–3 contains mainly speculative estimates of Li2O reserves and average concentrations 

of Ta2O5, rubidium and cesium calculated to a depth of 100 m. The calculations appear to be based on 

surface exposures and samples, as there are no indications of drilling, trenching, or underground 

workings. It is unclear when the information is shown as “NA” if there were no analyses requested or 

the analyses were below detection limits. The calculated reserves include only a few of the pegmatite 

deposits. It is unclear if these calculations represent only the perceived economic deposits or only the 
Chapter 24A. Summary for the Mineral Information Package for the Nuristan Rare-Metal Pegmatite Area of Interest 1645

deposits investigated in detail. Unevaluated resources are probably much larger. No reserves are 

available for the gemstone-bearing pegmatites.

Table 24A–3.

[Data are from United Nations Economic and Social Commission for Asia and the Pacific (1995), Orris and Bliss (2002), and 

Abdullah and Chmyriov (2008)] 

Speculative rare-metal reserves calculated to a depth of 100 meters and rare-metal grades. 

Pegmatite Li2O (metric tons) Li2O (weight percent) Ta2O5 (weight percent) Rb and Cs (weight percent)

Pasgusta 1,050,000 2.14 0.002 to 0.007 < a few hundredths

Drumgal 253,000 1.38 to 1.58 0.03 NA

Jamanak 450,000 1.83 0.006 0.02

Pasgusta-under 124,000 2.2 NA NA

Pashki 127,000 1.46 to 2.1 0.01 to 0.02 0.01 to 0.02

Yorigal 130,000 NA NA NA

Total 2,123,000

Figure 24A–6. Section A-B through the Darrahe Pec (Darai-Pich) deposit (modified from Fenogenov and 

Musazai, 1989). (Many maps and diagrams in the Russian literature lack vertical and horizontal scales.)

Figure 24A–7. Proposed vertical zoning of pegmatite mineralogy at the Darrahe Pec (Darai-Pich) deposit 

(modified from Fenogenov and Musazai, 1989). (Many maps and diagrams in the Russian literature lack vertical 

and horizontal scales.)
1646 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

Figure 24A–8. Schematic distribution of pegmatite zoning peripheral to a granitic source (modified from Trueman 

and Černý, 1982).

24A.8 Genesis of the Pegmatite Deposits

Mapped zoning patterns and the pegmatites’ mineralogy and geochemistry, noted above, indicate 

that the pegmatites are related to fertile, two-mica granites of the Oligocene-age Laghman intrusive 

complex.

Studies regarding genesis of the rare-metal types of pegmatites have evolved considerably during 

the past 30 years (Crouse and Černý, 1972; Stewart, 1978; Černý, 1982a,b, 1991a,b, 2005; Černý and 

Meintzer, 1988; Page and Page, 1998; Černý and Ercit, 2005; Linnen and Cuney, 2005; London, 2005, 

2008; Stilling and Černý, 2006). Further discussions regarding the genesis and evolution of the 

pegmatites in this part of Afghanistan must wait for more detailed mineralogical and geochemical data.

24A.9 Further Evaluation of Pegmatites

Further evaluation of the pegmatites should involve more detailed work on the known 

pegmatites, as well as exploration and documentation of pegmatites for which there is little or no 

information. Selected chemical analyses for potassium, rubidium, and cesium of blocky K-feldspars 

demonstrate enrichment trends that could be used to distinguish those pegmatites or pegmatite fields that 

may be enriched in lithium, cesium, beryllium, and tantalum or to define which pegmatite fields or 

pegmatites may or may not be economic (Trueman and Černý, 1982). Similar results are demonstrated 

for chemical analyses of muscovite (Cocker, 1992). 
Chapter 24A. Summary for the Mineral Information Package for the Nuristan Rare-Metal Pegmatite Area of Interest 1647

Figure 24A–9. Geologic map and cross sections A-B and C-D of the Nilaw-Kulam pegmatite field (modified from 

Rossovskiy, 1981b).
1648 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

Figure 24A–10. Block diagram showing relations between rock structure and lithology with pegmatite orientations 

and pegmatite zone morphologies (modified from Bogatskiy and others, 1978). (Many maps and diagrams in the 

Russian literature lack vertical and horizontal scales).

Exploration “guidelines” for rare-metal pegmatites have been nonexistent until recently, because 

exploration has been limited to a few companies that have an interest in the development of these 

pegmatites. There are only a few published references regarding exploration for these types of 

pegmatites (Selway and others, 2005; Trueman and Černý, 1982). Specific guidelines for lithium-, 

rubidium-, and cesium-bearing pegmatites are not published but can be deduced from the following 

suggested exploration guidelines for generally tantalum-rich pegmatites (Selway and others, 2005): 

1. Large, tantalum-bearing pegmatites tend to occur in proximity to regional faults. 

2. The source for rare-metal pegmatites is more likely to be peraluminous fertile granite, and the 

majority of tantalum-rich pegmatites occur within 10 km of these types of fertile granite. 

Exceptions to this observation are the Greenbushes and Tanco pegmatites, where a source granite 

has not been located. 

3. Rare-metal pegmatites commonly occur in greenschist to amphibolite metamorphic grade. 

4. Amphibolites and metamorphosed ultramafic rocks are the most common host rock for 

world-class tantalum-bearing pegmatites.

5. The host rocks may be metasomatized in the vicinity of tantalum-rich pegmatites with the more 

common minerals including holmquistite (a lithium-bearing amphibole), (rubidium, cesium)-rich 

biotite, and tourmaline. Muscovite and garnet (almandine) may also occur in metasomatic 

aureoles.

6. Tantalum-bearing pegmatites generally contain spodumene or petalite as the dominant 

lithium-bearing mineral.

7. Spodumene is the most common lithium-bearing mineral in tantalum-rich pegmatites, although 

lepidolite, amblygonite, lithiophilite, petalite, eucryptite, and pollucite may be present or 

important lithium phases. The most important cesium-bearing mineral is beryl.

8. The most common tantalum ore minerals include manganotantalite, manganocolumbite, 

wodginite, and microlite. Other ore minerals include tapiolite, stibiotantalite, ixolite, and 

simpsonite. Tantalum-rich cassiterite is commonly associated with tantalum oxides in tantalum 

deposits. 
Chapter 24A. Summary for the Mineral Information Package for the Nuristan Rare-Metal Pegmatite Area of Interest 1649

9. Enrichment of tantalum tends to occur in the albite-rich zone, commonly with an aplite texture, 

and mica-rich zones such as the cleavelandite plus lepidolite zone. Tantalum-oxide minerals 

within aplites tend to be fine grained, whereas they are coarse grained in spodumene zones.

24A.10 Summary of Potential

Soviet geologists documented the geology, mineralogy, and geochemistry of the pegmatite fields 

in mountainous terrain with difficult access. The information that they obtained suggests the pegmatites 

in the Nuristan rare-metal pegmatite AOI may have a high probability for rare metals. However, much 

remains unknown about the geochemistry, mineralogy, internal mineral zoning, zoning patterns within 

pegmatite fields, or pegmatite groups and structural details of the pegmatites. Details essential for 

consideration of deposit development are lacking.

The pegmatites in the Nuristan rare-metal pegmatite AOI are genetically and spatially related to 

nearby fertile, two-mica granites of the Oligocene-age Alingar Pluton. Further studies and evaluations of 

the pegmatites should focus on the suggested techniques and guidelines noted above. Also, knowledge 

of the zoning relations and of the structural orientation preferences of the pegmatites in each field would 

be useful for purposes of evaluation and exploration.

The main physical difficulties to assessing the mineral resources found in pegmatites of the 

Nuristan rare-metal pegmatite AOI include the physical access to the mountainous terrain of this area.

The road network into this region was damaged during the Soviet occupation of Afghanistan during the 

1980s (Bowersox and Chamberlain,1995). Access to many of the pegmatites noted at the time was by 

jeep road to a certain point and then on foot for tens of kilometers on rough trails and over the few 

bridges over narrow gorges (Bariand and Poullen, 1978; Bowersox and Chamberlain,1995).

Development of mining operations will require significant improvements to transportation network, a 

trained workforce, and dependable power and water supplies.

24A.11 References Cited

Abdullah, S., and Chmyriov, V.M., editors in chief, 2008, Geology and mineral resources of 

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