Chapter 2A. Summary of the Aynak Copper, Cobalt, and 

Chromium Area of Interest

Contribution by Cliff D. Taylor, Stephen G. Peters, and David M. Sutphin

Abstract

This report summarizes and interprets available data for the Aynak copper, cobalt, and chromium 

area of interest (AOI) and its subareas from joint geologic and compilation activities conducted during 

2009 to 2011 between the U.S. Geological Survey, the U.S. Department of Defense Task Force for 

Business and Stability Operations, and the Afghanistan Geological Survey. 

Numerous copper-cobalt and several chromium, talc-magnesite, and asbestos target zones are 

present in the Aynak AOI, located in southern Kabul, northern Logar, and Wardak Provinces. The AOI 

derives its name from the world-class Aynak copper-cobalt deposit that is currently estimated to contain 

240 million metric tons of ore at 2.3 percent copper. An estimate of the contained cobalt resource is not 

available due to insufficient assays; however, cobalt content of ores ranging from 0.015 to 0.3 percent 

have been reported and may represent significant added value. 

Aynak belongs to a class of deposits hosted in sedimentary rocks that are commonly laterally 

continuous over extensive areas. The presence of the Aynak deposit, several smaller deposits, and more 

than 40 prospects and occurrences is indicative of the significant future potential of the area for the 

discovery of additional economically important copper-cobalt deposits. The known deposits and 

prospects occur at the surface within complexly folded Neoproterozoic strata. Structural analyses 

suggest that the four main clusters of deposits are exposed in the crests of folds and that this pattern may 

be useful to project exploration for similar deposits under younger cover. The two southern deposit 

clusters contain the Aynak and Jawkhar-Darband-Kuhndara deposits which were the subject of a 

mineral tender package that was awarded to China Metallurgical Group Corporation. The two northern 

clusters remain open to mineral exploration and are included within the four copper-cobalt subareas 

described in this report. The northern areas require additional geological mapping, geochemical and 

geochronological sampling, data compilation, and geophysical studies to better delineate the favorable 

Neoproterozoic host rocks. 

Discovery of additional copper-cobalt deposits in the Aynak AOI would benefit in the early 

stages of exploitation and production from the ongoing infrastructure development at the Aynak deposit 

and the close proximity of the area to Kabul. With easy access to transport corridors, local labor sources, 

and the materials supply center in Kabul, it is reasonable to expect that medium-sized deposits or several 

smaller deposits in aggregate could be put into production with short lead times, short payback periods 

and, in time, likely lead to larger mining ventures. 

The occurrence and minor past exploitation of podiform chromite deposits, talc-magnesite, and 

asbestos in the Logar Ophiolite Complex in the Logar Valley just southwest of the Aynak deposit are of 

lesser importance to the economic recovery of Afghanistan. Podiform chromite deposits are typically 

small and do not represent a significant target for future exploration. However, recent documentation of 

platinum group elements in the Logar chromitites is of interest and could be amenable to small-scale 

mining if significant quantities of platinum group elements are identified. Additional sampling of the 

known chromite deposits and geochemical analyses are required to investigate this potential.
Chapter 2A. Summary of the Aynak Copper, Cobalt, and Chromium Area of Interest 37

2A.1 Introduction

The Aynak copper, cobalt, and chromium area of interest (AOI) is located in eastern Afghanistan 

in southern Kabul, northern Logar, and Wardak Provinces and includes parts of the Maydan Shahr, 

Nirkh, Chahar Asyab, Bagrami, Musayi, Khaki, Jabbar, Pull Alam, and Muhammad administrative 

districts. The area of the main Aynak AOI is 3,439.37 square kilometers (km2

), which contains five 

subareas. Four of the subareas, Kelaghey-Kakhay (27 km2

), Bakhel Charwaz (40 km2), Yagh-Darra 

Ghul-Darra (57 km2), and Kharuti Dawrankhel (66 km2) are prospective for copper-cobalt deposits. A 

fifth subarea, Logar valley (1,013 km2), is prospective for chromite and possibly platinum group element 

(PGE) deposits (fig. 2A–1).

Figure 2A–1.

Mineral deposit types that may be present in the Aynak AOI are sediment-hosted copper (cobalt) 

deposits, secondary (transported) copper deposits, podiform chromite deposits, serpentine-hosted 

asbestos deposits, and talc-magnesite deposits. In addition, podiform chromite deposits have the 

potential to contain PGEs. 

Location of the Aynak copper, cobalt, and chromium area of interest and subareas. 

Most existing mineral resource information has been gathered from reports written between the 

early 1950s and about 1985 by geologists from the Union of Soviet Socialist Republics (USSR) and its 

eastern European allies who provided Afghanistan with technical assistance. This previous information, 

combined with a preliminary nonfuel mineral resource assessment by the U.S. Geological Survey in 

2007 (Peters and others, 2007), provided much of the factual basis for technical work during 2009 

through 2011. During this period, Afghan Geological Survey crws were busy gathering new data on 

other less well prospected AOI’s, and only a single reconnaissance visit to several of the Aynak subareas 

was made by personnel of the USGS (figs. 2A–2 and 2A–3). The Logar subarea was not visited.

Resulting new data are, therefore, extremely limited and this current summary is compiled mainly from 

pre-existing sources. The following English language summaries were relied upon heavily: the geology 

and exploration of the Aynak and western Aynak areas by Russian workers released in the Aynak 

Information Package by the Afghan and British Geological Surveys (British Geological Survey 

2005a,b,c); the USGS preliminary nonfuel mineral resource assessment of Afghanistan (Peters and 

others, 2007); geological mapping in the Kabul North and Kabul South quadrangles at 1:100,000 scale 

(Bohannon, 2010a,b); and a recent paper on the chromite and PGE resources of the Logar Ophiolite 

Complex (Benham and others, 2009). The Aynak AOI and subareas also are thought to be likely to 

develop near-term mineral production. Additionally, some deposits in the Aynak AOI and subareas are 

near-surface bodies with promising metallurgical and mining characteristics.
38 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

Figure 2A–2. General aerial view of the north Aynak area. Photograph by Ted Theodore, U.S. Geological Survey. 

2A.2 Geology

The Aynak AOI and subareas are located within the Kabul tectonic block, one of many 

fragments of ancient continental crust interleaved with oceanic crust that was trapped between the 

Eurasian and Indian cratons during closure of the Tethyan sea from late Paleozoic to Cretaceous times 

(Tapponnier and others, 1981). Bounded on both the west and east by major terrane-bounding faults, the 

Kabul block is a north-northeast trending, lenticular-shaped sliver about 200 kilometers (km) long and 

50 km wide (British Geological Survey, 2005a). The block has a broadly anticlinal structure that 

exposes a core of Precambrian metamorphic rocks flanked by Late Paleozoic and Mesozoic rocks. 

Within the Kabul block, the main structural features are the Kabul Anticline Elevation and the Aynak 

Syncline Zone (British Geological Survey, 2005a). The Kabul Anticline Elevation is in the northern part 

of the block and is about 50 km wide and trends northwesterly. The northeastern limb dips at 40 to 

50 degrees and the southwestern limb dips at 70 to 80 degrees. The Aynak Syncline Zone, situated to the 

south of the Kabul Anticline Elevation, is elongated in an east-west direction, and is 60 km long and up 

to 20 km wide. The Aynak Syncline Zone hosts most of the copper deposits in the Kabul block (British 

Geological Survey, 2005b). 

Precambrian crystalline basement rocks in the Aynak syncline zone consist of amphibolite facies 

and higher grade metamorphic rocks of the Paleoproterozoic Sherdarwaza series and the (assumed) 

Neoproterozoic Kharog and Weyalati Formations, all of which are intruded by small lenticular and 

stock-like metamicrogabbro and migmatitic granite bodies (British Geological Survey, 2005b; 

Bohannon, 2010b; fig. 2A–4). The Sherdarwaza series consists of gneiss, migmatite, and schist with 

lesser amphibolite, quartzite, and marble. These lithologies occur in rhythmic sequences of basal 

quartzites upwards into gneisses, mica schists, amphibolites, and marbles. Individual sequences vary 
Chapter 2A. Summary of the Aynak Copper, Cobalt, and Chromium Area of Interest 39

from several meters to several tens of meters for a total thickness of more than 1,900 meters (m) in the 

central Kabul block (British Geological Survey, 2005b). The Kharog Formation conformably overlies 

the Sherdarwaza series, generally shares the same spatial distribution, and mainly consists of gray to 

light-gray quartzite that is interbedded at the base with conglomerates and with schist, gneiss, 

amphibolite, and marble in the upper parts of the formation. The nonquartzite layers in the upper part 

share similar composition, texture, and metamorphic grade with counterpart lithologies in the 

Sherdarwaza series. The Kharog Formation is up to 2,500 meters (m) thick (British Geological Survey, 

2005b; Bohannon, 2010b). The Welayati Formation overlies and is conformable with the Kharog 

Formation and is distributed throughout the Aynak District and northern Logar valley. The Welayati 

formation consists of a basal schist, a middle amphibolite, and alternating schist and amphibolite in the 

upper part as well as plagiogneisses, quartzites, and marbles. The Welayati Formation is 1,200 to 

1,500 m thick (British Geological Survey, 2005b; Bohannon, 2010b). 

Figure 2A–3. General view of the Precambrian metamorphic rocks (background) and flat-lying Neogene alluvium 

(foreground) in the north Aynak area. Photograph by Ted Theodore, U.S. Geological Survey. 

Recent uranium/lead-zircon (laser ablation) geochronological studies of amphibolitic schist and 

gneiss from the Sherdarwaza series gave Paleoproterozoic ages of 2,383 and 2,378 Ma, respectively 

(Bohannon, 2010b). The schist sample indicates that a metamorphic overprint occurred at 1,820 Ma, 

which obscures the origin of the protolith. Possibilities include a mafic igneous rock emplaced at 

2,394 Ma or a mafic metasediment with a variety of detrital zircon sources. The ages of the Kharog and 

Welayati Formations are not well documented, but they are assumed to be of Neoproterozoic age by 

Bohannon (2010b). The high-grade metamorphic rocks of the Sherdarwaza series and Kharog and 

Welayati Formations may be the crystalline basement of the northern Indian plate (Bohannon, 2010b). 

In the Aynak AOI, the older, high-grade Proterozoic basement rocks are overlain unconformably 

by a lower grade greenschist facies carbonate-clastic and volcanosedimentary cover sequence of 
40 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

Neoproterozoic (Vendian) to Cambrian age. The lower calcareous schist is named the Loy Kwar 

Formation and is the main host rock for the copper-cobalt deposits in the Aynak syncline zone. The 

conformably overlying volcanosedimentary schist is called the Gulkhamid Formation. The age of these 

units is uncertain and is based upon fragments of Neoproterozoic stromatolites in the Loy Kwar 

Formation. The presence of the algea Tannuofia (stomatolite tannuofia)

The Loy Kwar Formation is widespread throughout the central part of the Kabul block and 

consists of a thick metasedimentary sequence of repetitive layers of dolomitic marble, carbonaceous 

quartz schist, and quartz-biotite-dolomite schist. The lower Loy Kwar Formation is lithologically 

variable with layers of basaltic conglomerate, actinolite schist, calcareous biotite-schist, fine-grained 

breccia, banded biotite schist, quartzite, and dolomitic marble. Pyrite, chalcopyrite, bornite, chalcocite, 

pyrrhotite, and traces of molybdenite are present near the base of the formation. Marble, sandstone, 

quartzite, and carbonate-rich schist make up the middle of the formation and are host to much of the 

bornite-rich ore at Aynak. The upper parts of the formation consist of carbon-quartz schist with dark 

gray dolomite intercalations and gray, fine-grained, banded dolomite marble (British Geological Survey, 

2005b; Bohannon, 2010b). Owing to the importance of the Loy Kwar Formation as a host for copper 

deposits, it has been more intensively studied and described than other rocks in the area. Resulting 

schemes for subdividing the formation have been inconsistent and confusing, with as many as seven 

members and numerous submembers designated by various previous workers. Many of the subdivisions 

are thin (2 to 6 m) and possibly laterally discontinuous, adding to the confusion (Bohannon, 2010b). A 

more detailed description, based upon seven members identified at the Aynak deposit and used in the 

Aynak Information Package (British Geological Survey, 2005a), is shown in figure 2A–5. 

 suggests that the unit may be 

early Cambrian, resulting in the commonly assigned Vendian/Cambrian age (British Geological Survey, 

2005b; Bohannon, 2010b). The Gulkhamid Formation is devoid of fossil remains and has apparently not 

been dated. Earlier reports correlated the Gulkhamid Formation with similar mafic schists of the 

Weyalati Formation (British Geological Survey, 2005b; Bohannon, 2010b). 

The Gulkhamid Formation has been poorly described by previous workers due to the assignment 

of these widespread rocks to the Weyalati Formation. It consists of metamorphosed intermediate 

volcanic rocks with conglomerate, metasandstone, and schistose tuff at the base and interstratified 

green-gray lava, tuff, breccia, and tuffaceous sandstone of andesitic to dacitic composition in the upper 

part. Primary volcanic textures and fabrics are preserved, and the measured thickness of the unit is about 

1,000 m, although geophysical data suggest it may reach thicknesses of 2,000 m (Kubatkin and others, 

1978; British Geological Survey, 2005b). 

Numerous small intrusive bodies occur in the Aynak AOI and consist primarily of plagiogranite 

porphyry and syenite porphyry. They mostly intrude the Weyalati, Loy Kwar, and Gulkhamid 

Formations and intrude the Sherdarwaza series to a lesser extent. They are thought to be of 

Vendian/Cambrian age (British Geological Survey, 2005b; Bohannon, 2010b). 

Phanerozoic sedimentary rocks are present in marginal areas of the Kabul block and 

unconformably overlie the variably metamorphosed Proterozoic basement rocks described above. These 

rocks are mostly Early Carboniferous to Early Permian and consist of carbonate and continental clastic 

platform sequences. These rocks are sparse in the Aynak AOI. The Carboniferous through Early 

Cretaceous sequence is about 5 km thick (British Geological Survey, 2005b). Poorly consolidated, 

coarse-grained fluvial and fluviolacustrine sediments cover large areas of the Kabul block where they 

fill intermontaine depressions. These units are referred to as the Latabang Formation and are of Miocene 

to Recent age (British Geological Survey, 2005). They reach a maximum thickness of 600 m (British 

Geological Survey, 2005) and cover extensive parts of the Aynak District, especially in the area between 

the Aynak and Darband deposits and in the vicinity of Kurdkabul and Dawrankel (Bohannon, 2010b). 

The Logar Ophiolite Complex (LOC) is located about 30 km south of Kabul and underlies an 

area about 65 km long by 45 km wide just west of the Aynak District and southwest of the copper-cobalt 

subareas described in this report. The LOC has a roughly ellipsoidal outcrop pattern elongated to the 

north-northwest and covers an area of about 2,000 km2 centered on the Logar Valley (figs. 2A–6 and 
Chapter 2A. Summary of the Aynak Copper, Cobalt, and Chromium Area of Interest 41

2A–7). The LOC is an obducted fragment of oceanic crust that was thrust over the Kabul block during 

the Himalayan orogeny. The LOC is bounded on the west by the steeply dipping, north-south trending 

Pagman Fault and is separated from the underlying autochthonous rocks of the Kabul block along its 

northern and northeastern boundaries by the Abparan thrust fault (Benham and others, 2009). The major 

rock types in the Logar Valley chromite subarea are serpentinized harzburgite and dunite with minor 

noritic dikes in the southernmost areas. 

In more detail, the LOC consists of several major lithostratigraphic units—a lower ultramafic 

complex, which is separated from a pillow lava complex by a thin gabbro unit, and dike complex (fig.

2A–8; Benham and others, 2009). The pillow lava complex is overlain by a volcanosedimentary 

sequence, which is in turn overlain by accretionary wedge sediments. The LOC is believed to be 

Cretaceous in age, because the lower part of the volcanosedimentary sequence has been dated as Early 

Cretaceous and the upper part as Late Cretaceous (Benham and others, 2009). 

The ultramafic complex mostly consists of dunite and harzburgite with minor lherzolite, 

wehrlite, serpentinite, and serpentinite breccias. The central part is cut by basaltic dikes ranging in 

composition from basalt to basaltic andesite which varies texturally to microgabbro and gabbro-diorite.

The upper part of the ultramafic complex consists of layered ultramafic and mafic rocks, including an 

uppermost melanocratic layered gabbro (fig. 2A–8; Benham and others, 2009). The ultramafic complex 

is about 2,800 m thick and is host to the podiform chromite deposits in the LOC. 

The pillow lava complex consists of dark gray-green, aphyric to porphyritic, spilitized, basaltic 

to andesitic pillow lavas with rare layers of volcanic breccia, tuff, aglomeratic tuff, and tuff breccia. The 

volcanic rocks are occasionally interlayered with radiolarite, hyaloclastite, and muddy limestone (fig.

2A–8; Benham and others, 2009). The pillow lava complex is about 1,700 to 1,800 m thick. The pillow 

lava complex was formed in a deep oceanic environment which is consistent with the ophiolite origin of 

the LOC (Benham and others, 2009). 

2A.3 Metallogeny of Sediment-Hosted Copper Deposits

Sediment-hosted copper deposits are a large and diverse group of mineral deposits that include 

some of the richest and largest copper deposits in the world (Gustafson and Williams, 1981; Kirkham, 

1989; Davidson and Large, 1998; Hitzman and others, 2005), such as the copper deposits of the Central 

African Copper Belt, which have produced in excess of 1 billion metric tons (Gt) of copper at an 

average grade of about 2.7 percent copper, as well as significant quantities of cobalt and silver (Selley 

and others, 2005). 

Sediment-hosted copper deposits are restricted to a narrow range of layers within a sedimentary 

sequence but do not necessarily follow sedimentary bedding. They formed after the host sediment is 

deposited, but in most cases, prior to lithification of the host. Mineralization is independent of igneous 

processes. Host rocks are of two types—low-energy calcareous or dolomitic siltstones, shales, and 

carbonate rocks of marine or lacustrine origin; and high-energy sandstones, arkoses, and conglomerates 

of continental origin. Low energy host rocks are thin-bedded to finely laminated and exhibit bacterial 

mat structures, stromatolites, fenestral structure, reef-building coral structures, mudcracks, crossbedding, 

and other features of tidal environments. High-energy host rocks exhibit conglomerate- and sandstonefilled channels, scour-and-fill structures, crossbedding, parallel lamination, mud rip-up clasts, and ripple 

marks. Deposits of two distinct types are formed in these host rocks, reduced facies copper and redbed 

copper. Depositional environments include highly permeable sediments in epicontinental shallowmarine basins near the paleoequator 

Proximity to sabkhas and other environments that produce high evaporation rates are also 

favorable factors. Halite, sylvite, gypsum, and anhydrite deposits occur in the same sedimentary 

sequences. Sandstone uranium, unconformity uranium, and Kipushi-type copper-lead-zinc deposits can 

occur in the same districts. In addition, the iron oxide copper-gold and basaltic copper deposit sub 

models may be applicable within some of the areas studied. 
42 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

Figure 2A–4. Geology and mineral occurrences of the Aynak copper-cobalt and chromium area of interest based on Russian sources (Peters and others, 

2007). 
Chapter 2A. Summary of the Aynak Copper, Cobalt, and Chromium Area of Interest 43

Figure 2.A–5. Diagram showing the detailed stratigraphy of the Loy Kwar Formation as described by the British 

Geological Survey (2005a) at the Aynak deposit and primary mineral zonation of the copper-cobalt orebodies 

(British Geological Survey, 2005a, after Zaycev and others, 1988).
44 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

Figure 2A–6. Map showing the geology and location of podiform chromite, asbestos, and talc-magnesite occurrences in the Logar Ophiolite Complex. 

Geology from Russian sources (Peters and others, 2007). 
Chapter 2A. Summary of the Aynak Copper, Cobalt, and Chromium Area of Interest 45

Figure 2A–7.

Deposits of the reduced-facies subtype (model 30b.1; Cox and others, 2003), also termed coppershale or stratiform copper deposits, are hosted by reduced-facies marine or lacustrine rocks, such as 

green, black, or gray shale; siltstone; thinly-laminated tidal facies or reefoid carbonate rocks; and 

dolomitic shale. The deposits consist of stratabound, disseminated copper sulfide minerals that occur in 

reduced-facies sedimentary rocks, which overlie, or are interbedded with, redbed sedimentary sequences 

or subaerial basalt flows. Copper is mobilized in the redbeds by oxidized brines and is derived from 

reduction of sulfate in marine or lacustrine sedimentary rocks (Davidson, 1965). Fine-grained clastic 

rocks and carbonate rocks host 69 percent of the deposits and occurrences (Lindsey, 1982; Cox and 

others, 2003). Organic carbon and finely disseminated pyrite are common constituents. Host rocks for 

16 percent of the occurrences are carbonaceous, bituminous, algal, or stromatolitic. Thick, subaerial 

basalt flows are sources of copper in a few deposits (Brown, 1984), and evaporite beds are sources of 

brine for many deposits. 

Landsat TM imagery showing the Logar Ophiolite Complex.
46 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

Figure 2A–8. Lithological section through the ultramafic complex and pillow lava complex of the LOC (Benham 

and others, 2009, after Nevretdinov and Mirzamon, 1979).
Chapter 2A. Summary of the Aynak Copper, Cobalt, and Chromium Area of Interest 47

The following summary of the process leading to the formation of a sediment-hosted copper 

deposit is based on Cox and others (2003). Such deposits are formed by fluid mixing in permeable 

sedimentary and (more rarely) volcanic rocks. Two fluids are involved: an oxidized brine carrying 

copper as a chloride complex, and a reduced fluid, commonly formed in the presence of anaerobic 

sulfate-reducing bacteria. For a sediment-hosted copper deposit to form, four conditions are required:

1. An oxidized source rock must be present. This rock must be hematite stable and must contain 

ferromagnesian minerals or mafic rock fragments from which copper can be leached. In Zambia,

erosion of an early formed porphyry copper deposit is thought to have contributed copper to the 

source rock. Typical source rocks are continental red sandstone, shale, conglomerate, and 

subaerial volcanic rocks. Marine volcanic rocks are unsuitable as source rocks, because they 

have not degassed their volatile components. The reduced sulfur, which is contained in marine 

volcanic rocks, precludes the formation of a hematite-stable environment. Leaching of copper 

from the source rock at moderately low pH may be described by equation 1.

Cu2O + 6 Cl-+ 2 H+ = 2 CuCl3

2-

+ H2

2. Following equation 1, a source of brine must be present that mobilizes copper. Evaporites are 

commonly interbedded with redbeds and act as brine sources, but any sedimentary environment 

in which evaporation exceeds rainfall will produce brines. Brines may also form by evaporation 

of sea water where connection with the open sea is restricted, as in rift valleys. The brines are 

generally rich in sodium, because other cations, potassium, calcium, and magnesium, are 

removed during the formation of clays, sulfates, and carbonates. Davidson (1965) directed 

attention to the coincidence of evaporite deposits with Phanerozoic stratabound sediment-hosted 

copper deposits in many parts of the world, and proposed that brine derived from evaporites was 

the transporting medium for copper and other metals.

O (1)

3. A source of reduced fluid to precipitate copper and form a deposit must be present. The 

chemistry of brine formation, as well as copper mobilization and precipitation, was described by 

Rose (1976) and Rose and Bianchi-Mosquera (1993). Reduced fluids can be derived from 

organic-rich shales and carbonate rocks, from pockets of liquid or gaseous hydrocarbons in the 

host sediments, or from any sedimentary fluid in equilibrium with pyrite. In equation 2,

copper-rich brine contacts organic material and produces native copper.

2 CuCl3

2-

+ 2 H2O + C = 2 Cu0+ 1 CO2 + 4 H++ 6 ClNote that HCl appears on the right of this equation and others below. This enables the solution of 

carbonates and the replacement of calcite cement by native copper.

(2)

Sulfide in the form of finely disseminated pyrite is commonly found in reduced host 

sediments. The amount of pyrite in typical black shale is insufficient to supply all of the sulfur in 

high-grade copper deposits. A more abundant source of sulfide is from reduction of sulfate by 

carbonaceous material, promoted by bacterial activity in the sediment (Sweeney and Binda, 

1989) (eq. 3).

SO4

2-

+ CH4 = S2-+ CO2 + 2H2

Reaction of chloride complex with sulfide produces chalcocite

O (3)

2 CuCl3

2-

+ S2-= Cu2S +6 ClSulfate ion is commonly abundant in brines derived from evaporates and may accompany 

copper-rich oxidized solutions. The following reaction (eq. 5) results when and where the brine 

mixes with reduced fluids:

(4)

2 CuCl3

2-

+ SO4

2-

+ CH4 = Cu2S + CO2 + 2 H2O + 6 ClAction of sulfate-reducing bacteria is required to drive this reaction at near-surface temperatures.(5)
48 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

4. Conditions must be favorable for fluid mixing. Haynes (1986a,b) concluded that most sulfide 

ores are precipitated within 50 centimeters (cm) of the sediment-water interface, because 

bacterial sulfate reduction below this depth is inhibited. Prelithification permeability in shale 

provides bedding-parallel sites for fluid mixing. Fluid pressures derived from sediment 

compaction is an important factor in fluid mixing, and deposits are most commonly situated at 

basin margins where mixing is most likely to take place.

Faulting or folding may produce a hydraulic head that causes one fluid to invade the site of 

another. Disruption of sedimentary sequences by salt intrusion can also promote fluid mixing (Jowett, 

1986; Avila-Salinas, 1990; Ruan and others, 1991).

A permeable host rock or other open space must be present in which the fluids can mix. 

Intergranular space in fine-grained sediments prior to compaction and lithification is a common site for 

deposition. Solution cavities in carbonate rocks are less common depositional sites (MacKevett and 

others, 1997). If any of these four conditions are not met, a deposit will not form, even in the most 

favorable rock environments (Haynes, 1986a,b; Sverjensky, 1987, 1989; Ruffell and others, 1997; Cox 

and others, 2003; Hitzman and others, 2005).

Many of the most important sediment-hosted copper deposits formed during the metallogenic 

period of the Neoproterozoic when most of the world’s continental masses were joined in the Rodinia 

supercontinent (Laznika, 1981; Kirkham, 1989; Kirkham and others, 1994). No Archean deposits are 

known. The Upper Proterozoic rocks and, especially, Neoproterozoic rocks are the most productive. 

Permian rocks in Europe and Lower Carboniferous rocks in Central Asia are less important. Other small 

deposits are found throughout the Phanerozoic.

2A.3.1 Economic Geology

The characteristics of sediment-hosted copper-cobalt deposits in the Aynak AOI are best 

exemplified by features of the Aynak deposit. The Aynak deposit is hosted in rocks of the Loy Kwar and 

Gulkhamid Formations that are folded into a complex asymmetric anticline. The exposed parts are about

4 km long and up to 2.5 km thick. As a result of folding, the Aynak deposit is divided into two parts, 

with the Central Aynak zone located on the shallow-dipping eastern limb of the Aynak anticline and the 

Western Aynak zone lying in the western end of the structure (Gusev and others, 1979; Chernov and 

Fenogenov, 1980; Yashchinin and Giruval', 1981; Zaycev and others, 1988; Akhmadi, 1992) (fig. 2A–

9).

Two types of ores are known: the bornite type (with subordinate chalcocite), which makes up the 

main orebody, and the chalcopyrite type, which is present above and below the main orebody. 

Transitions between the two ore types display a rhythmic zoning, corresponding to the compositional 

layering of the sedimentary host rocks. The upper parts of the orebody are hosted within carbonaceous 

quartz-sericite-biotite schists, sandstones, and breccia, and they contain chalcopyrite, pyrite with 

sphalerite, and molybdenite. This upper part is underlain by sandstone, conglomerate, breccia, and 

dolomite, and it is dominated by bornite with lesser chalcopyrite, magnetite, molybdenite, and cobaltite. 

The lower parts of the orebody are hosted in carbonaceous quartz-dolomite schists with breccia, and 

they contain chalcopyrite and pyrrhotite with lesser pyrite, cobaltite, siegenite, and sphalerite 

(Yurgenson and others, 1981).

Cobalt concentrations in the Aynak copper ores that contain cobaltite range from thousandths of 

a percent to 0.3 percent cobalt. Cobalt minerals are present mainly in the chalcopyrite ores, pyritechalcopyrite, and bornite-chalcopyrite ores, where concentrations of cobalt are between 0.015 to 

0.018 percent cobalt. Cobaltite, the most common cobalt mineral in the deposit, occurs as dispersed 

disseminated crystals and aggregates that are 0.05 to 5 millimeters (mm) in size. The main occurrences 

of cobaltite are in the lower parts of the main ore body in chalcopyrite ores. Cobaltite also is present in 

the upper parts of the main orebody. Cobaltite in the bornite-chalcopyrite ores is associated with 

linneite, smaltite, carrolite, and cobaltpentlandite. Spatial distribution of cobalt minerals in the orebody 
Chapter 2A. Summary of the Aynak Copper, Cobalt, and Chromium Area of Interest 49

is related to the compositional variation of the layers in the host rocks and, therefore, also with the 

zoning of the copper minerals (Yurgenson and others, 1985).

2A.3.2 Greater Aynak Subarea

2A.3.2.1 Exploration History

The Aynak deposit and the surrounding areas were explored in the 1960s and 1970s. The first 

copper occurrences in the Darband area were discovered in 1971 (Denikaev and others, 1971). The main 

exploration work in the Aynak area started in 1974 and ended in 1978. In addition to drilling, 

geochemistry and ground geophysical methods were employed. During the same time period, about 

40 prospects with similar characteristics were identified, some that have small measured or estimated 

resources (Afghanistan Geological Survey, 2006a).

2A.3.2.2 Known Deposits

Aynak, the largest and best known sediment-hosted copper deposit in Afghanistan, is a worldclass copper orebody located about 30 km southeast of Kabul. The copper mineralization is stratabound 

and consists primarily of chalcopyrite and bornite disseminated in dolomitic marble and quartz-biotitedolomite schist of the Neoproterozoic (Vendian)-Lower Cambrian Loy Khwar Formation. Two major 

ore zones at Aynak Central and Aynak West were delineated by more than 30,000 m of drilling. 

(Plotnikov and Slozhenikin, 1968; Slavin and others, 1972; Chmyrev and others, 1976; Chmyrev and 

Azmi, 1977; Sidiki, 1978; Yurgenson and others, 1981, 1985).

The Aynak orebody can be classified as a sediment-hosted copper deposit, that is believed to 

have been formed by reactions between evaporitic brines and seawater circulating through underlying 

volcanic rocks that supplied the copper in the deposit. Some of the limestones and marls in the Loy 

Khwar Formation contain abundant carbon, probably former organic material that reacted with 

ascending solutions to fix copper sulfide minerals.

In addition to the Aynak deposit, numerous other sediment-hosted copper occurrences and 

prospects are present in the area, such as the Darband and Jawkhar prospects, which are east and north 

of the Aynak deposit, respectively. Considerable exploration was undertaken by Soviet geologists on a 

number of these prospects (United Nations Economic and Social Commission for Asia and the Pacific, 

1995; Afghanistan Geological Survey, 2006a,b).

A summary of known resources in the Aynak ore field (Abdullah and others, 1977; Ministry of 

Mines, written commun., 2007) is discussed below and the resources are listed in table 2A–1.

In 2006, the USGS and the AGS conducted a mineral assessment of copper resources in 

Afghanistan (Ludington and others, 2006; Peters and others, 2007) that resulted in the delineation of an 

area favorable for the discovery of additional copper deposits in the Aynak AOI. The favorable tract was 

designated as sedcu01-f1 and contained four separate prospective tracts delineated on the basis of 

mineral occurrence clustering, geology, and structure. Two of these favorable tracts, sedcu01-p1 

Yagh-Darra Ghul-Darra, corresponding to the Yagh-Darra Ghul-Darra subarea, and sedcu01-p2,

corresponding to the Kelaghey-Kakhay, Bakhel Charwaz and Kharuti Dawrankhel subareas, are 

described in this report. Two more, the p3 Aynak, and p4 Jawkhar-Darband-Kuhndara favorable tracts, 

were designated to the south. Subsequently, the favorable tracts of Aynak and Jawkhar-DarbandKuhndara were the subject of a mineral tender by the Afghan government, which was awarded to the 

China Metallurgical Group Corporation. The four prospective tracts contain numerous sediment-hosted 

copper deposits in addition to Aynak. Each prospective tract may represent a folded surface, where 

mineralization appears to be concentrated near the crests of complex folds (figs. 2A–10, 2A–11, and 

2A–12).
50 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

A 5-km-long prospective area (tract sedcu01-p3) was delineated around the Aynak deposit and 

the Akarkhel deposit to the northwest (figs. 2A–11a and 2A–12a). The Aynak deposit lies in the axis of 

the east trending Aynak anticline. The tract was drawn to include the stratigraphic extensions of the 

Aynak anticline.

2A.3.2.3 Aynak-Akarkhel

Several resource estimates have been reported for the Aynak deposit, which vary depending on 

the area estimated, the resource category, data used, and the estimator. Exploration at Aynak includes 

more than 150 boreholes, 70 trenches, 9 adits, and surface geological and geophysical surveys (Kubatkin 

and others, 1978; Kolotov and others, 1981; Karim and others, 1992). At a cutoff grade of 0.4 percent 

copper, the main orebody at Central Aynak extends 1,850 m along strike, 1,200 m downdip, and has a 

maximum thickness of 210 m. Based on a similar cutoff grade, the main body at Western Aynak extends 

2,230 m along strike, 1,640 m downdip, and has a maximum thickness of 214 m (Chmyrev and others, 

1977; Akocdzhanyan and others, 1977; Yashchinin and others, 1978, fig. 2A–9). “Industrial reserves” in 

the central sector are 4.83 million metric tons (Mt) with 2.37 percent copper using a 0.7 percent copper 

cutoff. Total reserve estimation of the Central Zone is 6.8 million metric tons of copper with an average 

copper content of 1.73 percent copper and a cutoff at 0.4 percent copper. Industrial reserve estimation of 

the western sector is 1.4 Mt of copper, with an average copper content of 1.61 percent and a cutoff grade 

of 0.4 percent copper. Total reserves in the western sector are 4.55 Mt with an average copper content of 

1.53 percent copper. The total resources at Aynak (central and western) is 11.33 Mt of copper with an 

average copper content of 1.64 percent at a 0.4 percent copper cutoff grade, corresponding to 690.9 Mt 

of ore (Ministry of Mines, written commun. 2007; Peters and others, 2007). Work conducted by the 

British Geologic Survey resulted in a resource estimation of 240 Mt of ore at 2.3 percent copper and 

includes several large orebodies and a number of smaller lenses (Afghanistan Geological Survey, 

2006a,b). 

The Akarkhel occurrence lies about 4 km northwest of Aynak and consists of a 50- to 60-m-thick 

zone of unknown length containing chalcopyrite, chalcocite, and malachite hosted in slate (Shcherbina 

and others, 1975). 

Table 2A–1. Deposits and prospects in the Aynak area with total contained copper, copper grade, and ore 

tonnage. [From Abdulla

Deposit

Aynak 

h and others, 1977; Peter

Copper, in metric tons

11,330,000

s and others, 2007] 

Grade weight, percent copper

1.64

Ore, in million metric tons

690.8 

Jawkhar 164,800 0.33–2.56 11.4 

Darband 665,700 0.79 84.3 

Taghar 86,800 0.18 48.2 

Katasang 42,100 1.04 3.0

Dashtak 8,200 1.67 0.5

Kelaghey

Total 

43,000

12,340,600

0.91

1.46

4.7

842.9
Chapter 2A. Summary of the Aynak Copper, Cobalt, and Chromium Area of Interest 51

Figure 2A–9. Geologic map and cross-section at the Aynak sediment-hosted copper deposit (Afghanistan 

Geological Survey, 2006a).
52 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

2A.3.2.4 Jawkhar-Darband-Kuhndara

An arcuate 25- to 30-km-long prospective area (tract sedcu01-p4) was delineated along the 

Logar-Kabul Province boundary to the east of the Aynak deposit (figs. 2A–11a, and 2A–12a). The 

outline of the prospective area approximates the area of an inferred antiform (figs. 2A–12b

At the Jawkhar (Dzhavkhar, Kawkhar) deposit, fifteen 150- to 440-m-long and 3- to 29-m-thick 

mineralized zones have average grades ranging from 0.49 to 1.20 percent copper, with a maximum 

grade of 2.43 percent copper. Mineralization occurs within albitized zones and consists of hypogene, 

chalcopyrite, and bornite, with auxiliary magnetite, ilmenite, pyrrhotite, and sphalerite. Supergene zones 

contain bornite, chalcocite, covellite, cuprite, native copper, and malachite. Detailed exploration at 

Jawkhar included 1:2,000-scale geological mapping, trenching, and the construction of 1,257 m of adits. 

A total of 1,635 channel samples and 1,191 other types of samples were taken for chemical analysis. 

This work resulted in the estimation of a resource of 79,700 metric tons (t) of copper with an average 

grade of 0.74 percent copper. Unfortunately, few exploration records for Jawkhar exist as they were 

destroyed or lost during the past 20 years (Kutkin and Gusev, 1977). The total resources in the C

) with the 

nose closing to the east. The tract contains the Jawkhar deposit in the northeastern part, the Darband 

deposit in the eastern part, and the Khundara occurrence in the western part. 

2

A number of mineral occurrences occur between the Jawkhar and Darband deposits in the 

northwestern part of the prospective area (figs. 2A–11

category for the Jawkhar, Dashtak, Sorbog, and Katasang areas are reported as 164,800 t of copper, with 

a copper content of between 0.33 and 2.56 percent copper (Ministry of Mines, written commun., 2007). 

a, and 2A–12a), including the Lalmi-Tanghi, 

Gezghay copper, Batkehl I and III, and Janguzay IV occurrences. The Lalmi-Tanghi occurrence consists 

of 200-m-long and 0.2- to 0.4-m-thick stratabound zones hosted within quartz-mica schist grading 1.35 

to 3.40 percent copper. The Gezghay copper occurrence consists of 5- to 15-m (up to 300-m)-long, 0.1-

to 1.0-m-thick mineralized lenses in micaceous calcareous schist containing quartz veins and veinlets 

that contain disseminated covellite, chalcocite, and chrysocolla grading 0.13 to 1.0 percent copper. The 

Batkehl I occurrence is within marbled limestone, quartzite, and biotite schists in four closely spaced 

zones, which together are 400 to 800 m long, 26 to 32 m thick, and contain disseminated chalcopyrite 

and malachite grading 0.5 to 1.94 percent copper (Shcherbina and others, 1975). The Batkehl III 

occurrence is hosted in amphibole-garnet slate in a 400-m-long and 6- to 30-m-thick zone containing 

disseminated chalcopyrite and covellite grading 0.4 to 2.0 percent copper. The Janguzay IV occurrence 

is hosted in marbled limestone, amphibolite, and slate and contains five 300- to 500-m-long and up to 

6-m-thick zones grading 0.4 to 4.46 percent copper. 
Chapter 2A. Summary of the Aynak Copper, Cobalt, and Chromium Area of Interest 53

Figure 2A–10. Maps showing the location of the Aynak AOI from Peters and others (2007) (a) Assessment map showing areas of potential and main 

prospects. (b) Permissive, favorable, and prospective areas for sediment-hosted copper overlain on the geology of Doebrich and Wahl (2006). 
54 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

Figure 2A–11. Maps showing location of favorable tract sedcu01-f1 and prospective tracts sedcu01-p1, p2, p3 and p4, Kabul and Logar Provinces. (a) 

Outline and location of favorable tract sedcu01-f1 and prospective tracts and location of known mineral occurrences and deposits. (b) Geology of tract 

sedcu01-f2. From Peters and others (2007). Units from Doebrich and Wahl (2006).
Chapter 2A. Summary of the Aynak Copper, Cobalt, and Chromium Area of Interest 55

Figure 2A–12. Maps showing location of stratabound copper occurrences in southern Kabul and northern Logar Provinces. (a) Location and names of 

main occurrences. (b) Structural interpretation of favorable tract sedcu01-f2 on the basis of existing formlines from Russian maps. Dark dotted lines show 

fold axial planes of antiformal and synformal structures. Grey dashed and solid lines are formlines showing the shape of these structures. Extensive internal 

folding is present within the rocks and is not shown. From Peters and others (2007).
56 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

The Darband copper deposit lies near the crest (or nose) of the inferred Jawkhwar-DarbandKuhundara antiform (figs. 2A–11a, and 2A–12b

A cluster of deposits is present south of the Darband deposit within the prospective area, 

including the Batkehl II and IV, Janguzay I, II, and III, and the Gughimayden stratabound mineral 

occurrences (figs. 2A–11

) that corresponds to the eastern extension of the axial 

plane of the Aynak anticline. The deposit is hosted in 70 to 80 degrees north-dipping silicified 

micaceous marble with interbedded biotite-amphibole schist and amphibolite of the Loy Khwar and 

Welayati Formations, and can be traced for 7,000 m along strike over a width of 100 to 1,000 m 

(fig. 2A–13). Mineralization at Darband occurs as disseminated-veinlets, and as aggregates containing 

chalcopyrite and bornite, with chalcocite, as well as pyrite, pyrrhotite, molybdenite, hematite, magnetite, 

and minor galena, sphalerite, cobaltite, arsenopyrite, nickel minerals, and gold. Bornite is the dominant 

ore mineral in the deposit, comprising 67 to 100 volume percent of the sulfide minerals. Supergene 

copper minerals are also present in the 150- to 200-m-thick oxidized zones, which consist of malachite, 

cuprite, covellite, azurite, and chrysocolla, gradually changing at depth to a mixed zone of native copper, 

chalcopyrite, and cuprite. About 25 stratabound mineralized zones have been delineated. A few zones 

are discordant and composed of silicified rocks and veinlets of quartz in faults or crush zones. 

Exploration work enabled division of the area into four prospects, designated Eastern Darband, Central 

Darband, Western Darband, and Lagernaya. The entire area was mapped at a scale of 1:2,000, and the 

mineralization was sampled by surface trenches that were initially spaced 100 m apart. Later trenches 

were 50 m apart. Eleven exploratory adits, totaling 9,062 m in length, were driven into the deposit at the 

Eastern, Central, and Western Darband prospects. Fifty-seven surface boreholes were drilled with a total 

length of 8,752 m. Of these, 14 boreholes were drilled in the Lagernaya prospect, and the remainder in 

Eastern, Central, and Western Darband. This work resulted in an estimate of 84.3 Mt of inferred or 

possible resources with 665,700 t estimated to contain copper, with an ore grade of 0.79 percent copper, 

using a cutoff grade of 0.4 percent copper (British Geological Survey, 2005c; Peters and others, 2007). 

Minchenok and others (1979) (Ministry of Mines, written commun., 2007) indicated that additional 

resources may be present beneath areas of Neogene sedimentary cover that were not explored (see also 

Denikaev and others, 1971; Chmyrev and others, 1977). 

a, and 2A–12a

The southwestern part of the Jawkhwar-Darband-Kuhundara antiform between the 

Gughimayden, Khundara, and Pachi mineral occurrences is covered by Neogene sediments. The Pachi 

occurrence, within strongly albitized rocks, is an 800-m-long, 4- to 49-m-thick zone and grades 0.9 to 

1.6 percent copper (Peters and others, 2007). The Khundara occurrence is within slate and marble, and 

consists of three mineralized zones that are between 200 to 300 m long and 10 to 20 m thick and grades 

0.8 to 1.6 percent copper (figs. 2A–11a, and 2A–12a; Peters and others, 2007).

). The Batkehl II and IV occurrences are hosted in biotitegarnet-amphibolite schists and both contain two zones about 250 to 450 m long and 5 to 9 m thick 

containing disseminated chalcocite, bornite, covellite, malachite, and azurite grading between 0.69 to 

0.96 percent copper. The Janguzay I occurrence is within amphibolite in a 500-m-long and up to 

6-m-thick zone grading 2.05 percent copper. The Janguzay II occurrence is within marbled limestone 

and slate and contains four zones that are 300 to 1,300 m long and 1.5 to 15 m thick grading 1.55 to 

3.28 percent copper. The Janguzay III occurrence is within amphibolite and consists of three 300- to

1,200-m long, 1- to 6-m-thick zones grading 0.2 to 3.0 percent copper. The Gughimayden occurrence is 

a quartz vein in marble that is 30 to 40 m long and 2 to 3 m thick, containing malachite and chalcopyrite 

that grades 0.84 percent copper (Shcherbina and others, 1975). 

2A.3.3 Kelaghey-Kakhay Subarea

The Kelaghey-Kakhay copper subarea lies in the northern part of the Aynak copper district (fig. 

2A–4). Surface exploration and mapping have identified signs of mineralization along a northeast 

trending zone in the central parts of the subarea coincident with a northeasterly trending range of hills 
Chapter 2A. Summary of the Aynak Copper, Cobalt, and Chromium Area of Interest 57

(figs. 2A–14 and 2A–15). The area may contain sediment-hosted copper deposits similar to Aynak at 

depth. A total of five separate occurrences have been identified.

Figure 2A–13. Simplified geologic map and cross-section of the Darband sediment-hosted copper deposit 

(British Geological Survey, 2005c, and Afghanistan Geological Survey, 2006b, based upon Minchenok and others, 

1977).

2A.3.3.1 Location

The Kelaghey-Kakhay copper-cobalt subarea is located 18 to 20 km south of Kabul in the 

Musavya District of Kabul Province and the Muhammad Agh District of Logar Province. An 

unimproved (tertiary) road accesses the villages of Katasang, Suryawun, and Shadkhana along the north 

side of the range. The villages of Dashtak (Loy Kalay) and Cagay are located in the valley on the south 

side of the range (fig. 2A–14). 

2A.3.3.2 Previous Work

The Kelaghey-Kakhay copper-cobalt subarea is in the southwestern part of prospective tract 

sedcu01-p2 (Peters and others, 2007; figs. 2A–11a and 2A–12a). The Kelaghey, Sorbog, Katasand, and 

Dashtak occurrences were evaluated by Kutkin and Gusev (1977). 

2A.3.3.3 Geology

The geology of the subarea (as mapped by Bohannon, 2010b) is dominated by the Weyalati 

Formation which makes up most of the outcropping rocks along the northeast trending range of hills that 

cuts through the center of the subarea (fig. 2A–14, 2A–15). This suggests that the dominant lithologies 

should be amphibolite facies schist, amphibolite, plagiogneisses, quartzites, and marbles. An outcrop in 
58 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

the southern valley floor at the Dashtak occurrence is mapped as the Loy Kwar Formation, and a thin 

strip of Loy Kwar Formation rocks are mapped along the southern margin of the range just to the south 

of the Kelaghey and Sorbog occurrences. Outcrops of undifferentiated Weyalati and Loy Kwar 

Formation rocks occupy the ridge crest between the Katasang and Sorbog occurrences and along the 

ridge crest at the Kakhay occurrence to the northeast as well as a large east-northeast trending band 

along the northern flank of the range. Presumeably, these rocks are represented by the lithologies of the 

Weyalati Formation mixed in with the repetitive layers of dolomitic marble, carbonaceous quartz schist, 

and quartz-biotite-dolomite schist that characterize the Loy Kwar Formation. A thin band of (assumed) 

Neoproterozoic intrusive rocks is exposed along the northeastern part of the range just north of the 

subarea boundary. 

2A.3.3.4 Known Deposits

No known deposits are present in the Kelaghey-Kakhay subarea.

2A.3.3.5 Prospects and Anomalies

The Kelaghey (Kalagay) copper occurrence lies in the far western part of the subarea. Limited 

exploration included geological mapping at 1:2,000 scale, trenching, and geochemical sampling. 

Mineralization is within quartzite and consists of disseminated bornite, chalcopyrite, and minor 

malachite hosted in dolomite marble and quartzite over a 1.5- by 40-m-size area. One prospecting trench 

contains an average grade of 0.79 percent copper over 7.1 m (Shcherbina and others, 1975; Kutkin and 

Gusev, 1977). 

Northeast of Kelaghey, the Sorbog (Sar Bagh) occurrence received limited exploration including 

1:2,000-scale geological mapping, trenching, and geochemical sampling. The 540-m-long and 11.8- to

49-m-thick (average 22.3 m) mineralized zone is hosted within albitized marble. Mineralization consists 

of disseminated bornite, chalcopyrite, chalcocite, covellite, and minor malachite. Resources were 

estimated to be 34,800 t of copper at an average grade of 0.91 percent copper and a cutoff grade of 

0.4 percent copper (Kutkin and Gusev, 1977). The Soviet survey concluded that the occurrence was 

“noncommercial.”

The Katasang occurrence is an 800-m-long, 3.6- to 13.8-m-thick (average 7.2 m) mineralized 

zone within steeply dipping, albitized marble containing disseminated bornite, chalcopyrite, chalcocite, 

and minor malachite. Limited exploration conducted at this site included 1:2,000-scale geological 

mapping, trenching, and geochemical sampling, and resulted in the calculation of a resource of 42,100 t 

of copper at an average grade of 1.04 percent copper (Kutkin and Gusev, 1977). The occurrence was 

classified as “noncommercial,” although more detailed exploration at depth was recommended. 

The Dashtak occurrence lies east of Kelaghey and is hosted within dolomitic marble in a 60- to

200-m-long and 1.2- to 17.3-m-thick oxidized zone that grades 1.67 percent copper containing bornite, 

chalcopyrite, and pyrite with secondary chalcocite, covellite, and cuprite. Exploration conducted at this 

site included 1:2,000-scale geological mapping, trenching, drilling of two boreholes totaling 212.6 m, 

and channel and core sampling. A resource was estimated to be 8,200 t of copper at an average grade of 

1.67 percent copper. Soviet geologists concluded that the occurrence has limited importance on its own 

but may have potential if the Aynak Deposit were to be developed. 

The Kakhay occurrence is located in the northeastern end of the subarea on the south side of the 

range facing the village of Cagay. Limited exploration included geological mapping at 1:2 000 scale, 

trenching, and geochemical sampling. Mineralization is represented by disseminated bornite, 

chalcopyrite, and minor malachite. Kakhay consists of two mineralized zones 200 and 250 m long and 

2.0 and 2.3 m thick, with average copper contents of 0.58 and 1.05 percent, respectively, and which are 

considered to have no economic importance (Shcherbina and others, 1975; Kutkin and Gusev, 1977). 
Chapter 2A. Summary of the Aynak Copper, Cobalt, and Chromium Area of Interest 59

2A.3.4 Bakhel-Charwaz Subarea

The Bakhel-Charwaz copper-cobalt subarea lies in the northern part of the Aynak copper district 

(fig. 2A–4). Surface exploration and mapping has identified signs of mineralization along an eastern

trending zone for about 8 km in the central part and also along the southeastern margin of the subarea 

(figs. 2A–15 and 2A–16). The area may contain sediment-hosted copper deposits similar to Aynak at 

depth. A total of nine separate occurrences have been identified.

Figure 2A–14. Geology and mineral occurrences of the Kelaghy-Kakhay copper-cobalt subarea. From Bohannon 

(2010b).
60 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

Figure 2A–15. Legend for figures showing the geology and mineral occurrences of the Kelaghy-Kakhay, BakhelCharwaz, Yagh-Darra Ghul-Darra, and Kharuti-Dawrankhel copper-cobalt subareas.

2A.3.4.1 Location

The Bakhel-Charwaz subarea is located about 10 to 15 km southeast of the City of Kabul in the 

Musavi and Khaki Jabbar Districts of the Kabul Province and the Muhammad Agh District of the Logar 

Province; no roads exist in this subarea. The mineral occurrences are located in a mountainous region 

near the villages of Zakhel and Baghgay (figs. 2A–16 and 2A–17). Surface workings of the Bagkhei and 

Zakhel II occurrences are distributed around the head of the valley to the north of the village of Zakhel, 

and the Zakhel I and Palanghar occurrences are located to the southwest and southeast of the village, 

respectively. The Barkhei, Charwazi III, and Charwazi IV occurrences are located in the mountains to 

the north, northwest, and southeast of the village of Baghgay. The Charwazi II and Charwazi I 

occurrences are located in the far northeasternmost corner of the subarea.

2A.3.4.2 Previous Work

The Bakhel-Charwaz copper-cobalt subarea is in the central part of prospective tract sedcu01-p2 

(Peters and others, 2007; figs. 2A–11a and 2A–12a). The Zakhel I and II occurrences have received 

limited exploration, including geological mapping at 1:2 000 scale, trenching, and geochemical 

sampling. Limited exploration at Palanghar consisted of 1:2,000-scale geological mapping, trenching, 

and geochemical sampling.
Chapter 2A. Summary of the Aynak Copper, Cobalt, and Chromium Area of Interest 61

2A.3.4.3 Geology

The geology of the subarea (as mapped by Bohannon, 2010b) is dominated by outcrop of 

undifferentiated Weyalati and Loy Kwar Formation rocks, especially in the northern, central, and eastern 

parts of the subarea (fig. 2A–16). This indicates that the dominant lithologies are probably amphibolite 

facies schist, amphibolite, plagiogneisses, quartzites, and marbles of the Weyalati Formation and 

repetitive layers of dolomitic marble, carbonaceous quartz schist, and quartz-biotite-dolomite schist of 

the Loy Kwar Formation (fig. 2A–18). 

Rocks of the Weyalati Formation underlie the undifferentiated Weyalati and Loy Kwar 

Formations in the southwestern quadrant of the subarea at and west of the Zakhel I occurrence, 

southwest of the Bagkhei occurrence, and surrounding the Palanghar occurrence in the south-central part 

of the subarea. A thin, east-west trending band of Weyalati Formation is present between the Bagkhei, 

Zakhel II, and Barkhei occurrences in the center of the subarea and in an area along the northern border 

of the subarea to the west of the Charwazi I and II occurrences. Neoproterozoic intrusive rocks are 

present to a greater degree in the Bakhel-Charwaz subarea and outcrop prominently in the west-central, 

central, and northeastern parts of the subarea. Neoproterozoic intrusive rocks are interbedded with the 

east-west trending strip of Weyalati Formation at the head of the valley between the Bagkhei and Zakhel 

II occurrences where they appear to be associated with most of the surface workings. A large mass of 

Neoproterozoic intrusive rocks to the west of the village of Baghgay may be associated with surface 

workings in the vicinity of the Charwazi III occurrence. 

A normal fault of unknown vertical displacement or direction of throw projects diagonally 

through the subarea for about 7 km along a northeastern trend from the Zakhel I occurrence through the 

northeastern corner of the subarea. All nine of the known occurrences in the subarea are distributed 

within a few kilometers of the fault, and the fault and the outcrop pattern of the mapped units in the 

subarea follow a northeasterly trend consistent with the perceived pattern of folding in the north Aynak 

region (Peters and others, 2007; fig. 2A–12b).

2A.3.4.4 Known Deposits

No known deposits are present in the Bakhel-Charwaz subarea.

2A.3.4.5 Prospects and Anomalies

The Bakhel-Charwaz subarea contains nine occurrences. From southwest to northeast they are 

named Zakhel I, Palanghar, Bagkhei, Barkhei, Charwazi III, Zakhel II, Charwazi IV, Charwazi II, and 

Charwazi I.

The Zakhel, Palanghar, Bagkhei, Barkhei, and Charwazi occurrences lie north of the Jawkhar 

deposit. The Zakhel I occurrence consists of two copper-bearing zones, 1 km long and 20 to 100 m 

wide, hosted in marble of Vendian-Cambrian age (presumeably the Loy Kwar Formation). Sampled 

intervals of 0.34 percent copper over 25 m, 0.53 percent copper over 90 m, and 1.06 percent copper over 

40 m were reported. The Zakhel II occurrence consists of two irregularly mineralized zones, one 500 m 

long and 2 to 10 m wide, and the second 1,500 m long and 20 to 35 m wide hosted in marble of 

Vendian-Cambrian age (presumeably the Loy Kwar Formation). Sampling in one of these zones 

determined copper values over an interval of 27 m grading 0.5 percent, and an interval of 32 m grading 

0.59 percent. The mineralized zones at both of the Zakhel occurrences contain malachite with bornite, 

chalcopyrite, and rare chalcocite and covellite (Shcherbina and others, 1975). Only a few samples 

contained copper concentrations above 1.3 percent copper, and the occurrences were considered to have 

no economic importance by Kutkin and Gusev (1977). 

The Palangar occurrence consists of a 750-m-long and 6.1- to 16.1-m-wide (average 11.4 m) 

stratiform zone containing disseminated chalcopyrite, chalcocite, and rare malachite hosted in dolomite 
62 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

marble and carbonaceous-mica-quartz schist. Details reported by Abdullah and others (1977) indicate 

that three copper-bearing zones 2 to 8 m wide and 70, 150, and 450 m long are present and that copper 

values in these zones average 0.55 to 3.18 percent. A resource in a central zone (up to 1 m depth) of 187 

t of copper was reported based upon limited exploration consisting of 1:2,000-scale geological mapping, 

trenching, and geochemical sampling. The occurrence was considered to have no economic importance 

(Kutkin and Gusev, 1977). 

The Barkhei (Baghgay) occurrence is hosted in marble and carbonate-mica schist of VendianCambrian age. It consists of two copper-bearing zones, 3 to 10 m in thickness and 400 and 500 m in 

length. In these zones, a 5-m interval contains 1.45 percent copper and a 4-m interval, 0.34 percent 

copper (Shcherbina and others, 1975; Abdullah and others, 1977). 

The Charwazi (Charwozi) occurrences are hosted in greenschist, slate and marble of VendianCambrian age. The Charwazi I occurrence consists of a copper-bearing zone 8 m wide and 100 to 150 m 

long averaging 1.3 percent copper. The Charwazi II occurrence consists of a copper-bearing zone 3 to 

5 m wide and 150 m long, with a 5-m interval containing 1.89 percent copper. The Charwazi III 

occurrence consists of a copper-bearing zone 1 m thick and 300 m long containing 0.48 percent copper. 

The Charwazi IV occurrence consists of a copper-bearing zone between 5 and 15 m wide and 400 m in 

strike length averaging 0.26 percent copper (Shcherbina and others, 1975; Abdullah and others, 1977). 

2A.3.5 Kharuti-Dawrankhel Subarea

The Kharuti-Dawrankehl copper-cobalt subarea lies in the northern part of the Aynak copper 

district (fig. 2A–4). Surface exploration and mapping has identified mineralization along an east-west 

trending 4-km-long range of hills in the south-central part, in the valley floor in the central part, and 

along the southwestern flank of the mountain range in the northeastern part of the subarea (figs. 2A–15 

and 2A–19). The area may contain sediment-hosted copper deposits similar to Aynak at depth. A total of 

seven separate occurrences have been identified.
Chapter 2A. Summary of the Aynak Copper, Cobalt, and Chromium Area of Interest 63

Figure 2A–16. Geology and mineral occurrences of the Bakhel-Charwaz copper-cobalt subarea (based upon 

Bohannon, 2010b).

2A.3.5.1 Location

The Kharuti-Dawrankehl copper-cobalt subarea is located 25 km southeast of Kabul in the of 

Khaki Jabbar and Bagrami Districts of the Kabul Province. An unimproved (tertiary) road accesses the 

valley floor through the mountain range on the northern border of the subarea and runs southward 

through the villages of Kurd-Kabul, Malik Khel and Khaki Jabbar before exiting the southeastern corner 

of the subarea. A second road forks off from the north-south road in the north-central part of the valley 

and exits through the eastern border of the subarea north of the village of Sheman Zay. The villages of 

Taghar, Mirza Khan Karez, Aynak, and Kharoti are located on the valley floor along the western side of 

the subarea (fig. 2A–19).

2A.3.5.2 Previous Work

The Kharuti-Dawrankehl copper-cobalt subarea is in the northeast part of prospective tract 

sedcu01-p2 (Peters and others, 2007; figs. 2A–11a and 2A–12a). The Chakari, Kharuti, Mirzakhan, and 

Dawankhel occurrences were evaluated by Shcherbina and others (1975) and Kutkin and Gusev (1977). 
64 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

Figure 2A–17. Aerial view of the Barkhei-Zakhel prospect area within the Bakhel-Charwaz subarea. Photograph 

by Ted Theodore, U.S. Geological Survey. 

2A.3.5.3 Geology

The geology of the subarea (as mapped by Bohannon, 2010b) is dominated by the Lataband 

series and recent alluvium of the Surficial series which cover the valley floor in the northwestern, 

central, southern, and southeastern parts of the subarea (figs. 2A–15, 2A–19, 2A–20). A fundamental 

transition between mapped geologic units can be observed in figure 2A–19, where rocks in the 

southeastern half of the subarea are almost exclusively the high-grade gneiss, migmatite, and schist with 

lesser amphibolite, quartzite, and marble of the Paleoproterozoic Sherdarwaza Formation, and rocks in 

the northwestern half are mapped as younger, lower grade, greenschist facies carbonate-clastic, and 

volcanosedimentary rocks of the Neoproterozoic cover sequence. Three major outcrop areas of 

Precambrian rocks are present in the subarea. An east-west trending range of hills in the southern part of 

the subarea hosts the Kharuti II, Khurdkabul, and Chakari occurrences (fig. 2A–19), in addition to 

numerous other surface workings, and is dominated by rocks of the Sherdarwaza Formation. 

Neoproterozoic intrusive rocks are present at the western end of the range and a small hill consists of 

Weyalati and undifferentiated Weyalati and Loy Kwar Formation rocks. Similarly, the northern and 

northeastern quadrants of the subarea contain a mountain range consisting of Sherdarwaza Formation 

rocks in the eastern part of the range, which host the Taghar and Dawrankhel occurrences.The western 

part of the range is dominated by rocks of the Weyalati Formation intruded by several large 

Neoproterozoic intrusive bodies. The hills in the west-central part of the subarea consist of Weyalati and 

undifferentiated Weyalati and Loy Kwar Formation rocks intruded by numerous small to medium-sized 

Neoproterozoic intrusions. The Kharuti I and Mirzakhan occurrences are located in Surficial series 

alluvium just to the east of these hills.
Chapter 2A. Summary of the Aynak Copper, Cobalt, and Chromium Area of Interest 65

Figure 2A–18. Photograph of laminated marble in the Bagkhei prospect area (GPS 34.34856° N, 69.28179° E) 

within the Bakhel-Charwaz subarea. Photograph by Ted Theodore, U.S. Geological Survey. 

2A.3.5.4 Known Deposits

No known deposits are present in the Kharuti-Dawrankehl subarea. 

2A.3.5.5 Prospects and Anomalies

The Kharuti-Dawrankehl subarea contains the Kharuti (Kharoti) I and II, Khurdkabul, Chakari, 

Mirzakhan, and Dawrankhel, and Taghar occurrences. The Kharuti I occurrence consists of a copperbearing zone 5 to 10 m wide and 200 m long in marble (thought to be of Vendian-Cambrian age by 

Shcherbina and others, 1975). The 10 m wide interval averages 0.99 percent copper. 

The Kharuti II occurrence is hosted in a marble-schist (thought to be of Vendian-Cambrian age 

by Shcherbina and others, 1975) and consists of nine 100- to 900-m-long, 3- to 35-m-wide copperbearing zones that grade between 0.15 and 0.94 percent copper (Shcherbina and others, 1975; Abdullah 

and others, 1977). In 2009, a team of USGS geologists visited the area of the Karuti II occurrence and 

reported their observations of a 300-m thick section of amphibolite facies mica schist, calcsilicate 

gneiss, marble, and mafic to felsic gneisses (amphibolite and quartzofeldspathic gneiss) of probable 

volcanic origin intruded by a 5-m-thick meta-aplite intrusion (figs. 2A–21 to 2A–23). Their observations 

of high-grade metamorphic rocks in the area are consistent with the mapping of Bohannon (2010b), 

which indicates the presence of the Paleoproterozoic Sherdarwaza Formation in this range of hills in 

contrast with the assumed Vendian-Cambrian age of rocks in the area reported by Shcherbina and others 

(1975). Additional detailed mapping and geochronological studies are required to resolve this conflict. 
66 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

The Khurdkabul occurrence consists of three copper-bearing zones with widths ranging from 5 

to 50 m and lengths from 800 to 900 m in marble, phyllite, micaceous carbonate, and garnet-mica schist 

(thought to be of Vendian-Cambrian age by Shcherbina and others, 1975). The mineralization consists 

of covellite, chalcopyrite, and chalcocite in irregular disseminations and veinlets. Average grades of 

0.18 to 0.36 percent copper are reported from 5- to 37-m-thick intervals (Shcherbina and others, 1975; 

Abdullah and others, 1977). 

The Chakari occurrence consists of a copper-bearing zone in marble (thought to be of 

Vendian-Cambrian age by Shcherbina and others, 1975). The zone is 200 m long, 3 to 5 m wide, and 

grades 0.2 percent copper.

The Mirzakhan occurrence consists of two copper-bearing zones, 10 to 35 and 10 to 20 m wide

and 800 and 500 m long, respectively A 35-m interval contains 0.24 percent copper and a 20-m interval, 

0.32 percent copper (Shcherbina and others, 1975). 

The Dawankhel occurrence is a 500-m long and 5 to 8 m wide copper-bearing zone that has been 

traced at the contact between marble and carbonate-mica schist (thought to be of Vendian-Cambrian age 

by Shcherbina and others, 1975) with an average grade of 1.1 percent copper. 

The Taghar occurrence is a large mineralized area hosted in micaceous carbonate rocks, phyllite, 

garnet-mica schist, and marble, and consists of 19 discontinuous copper-bearing zones that range from a 

few hundred meters to 6,000 m long and several meters to 200 m wide. The irregular zones contain 

chalcopyrite, bornite, chalcocite, covellite, malachite, and azurite in veinlets, pods, and disseminations. 

Mineralized sections between 3 and 25 m and 40 to 70 m wide (and up to 100 to 200 m wide) grade 1 to 

2.64 percent copper (Shcherbina and others, 1975). Resources at the C2 category level cover an area of 

31 km2 and are estimated to be 86,800 t of copper at a grade of 0.18 percent (Ministry of Mines, written 

commun., 2007; Peters and others, 2007). 

2A.3.6 Yagh-Darra Ghul-Darra Subarea

The Yagh-Darra Ghul-Darra copper-cobalt subarea lies in the mountainous northwestern part of 

the Aynak copper district (fig. 2A–4). Surface exploration and mapping has identified mineralization 

along an east trending zone in a 6 km2 area in the northwestern part and additional occurrence in the 

eastern part of the subarea (figs. 2A–15 and 2A–24). The area may contain sediment-hosted copper 

deposits similar to Aynak at depth. A total of three separate occurrences have been identified.

2A.3.6.1 Location

The Yagh-Darra Ghul-Darra copper subarea lies 10 to 20 km southeast of Kabul in the Bagrami, 

Musayi, and Khaki Jabbar Districts of the Kabul Province. The majority of the area consists of steep, 

mountainous terrain and there are no roads in the area. The village of Gul Dara is located near the head 

of the valley in the southwestern corner of the subarea about 2 km south of, and at the foot of the ridge 

below, the Ghuldarra II occurrence (fig. 2A–24). 

2A.3.6.2 Previous Work

The Yagh-Darra Ghul-Darra copper copper-cobalt subarea is centered on the prospective tract 

sedcu01-p1 of Peters and others (2007; figs. 2A–11a and 2A–12a). The mineralized trend in the YaghDarra Ghul-Darra subarea is probably the hanging wall limb of equivalent folded strata to the south that 

defines the east-northeast trending sequence of prospects and occurrences contained within the 

Kelaghey-Kakhay, Bakhel Charwaz, and Kharuti Dawrankhel subareas (figs. 2A–11a, and 2A–12b).

The southern limb of folded strata defines a 25-km-long, 3- to 4-km-thick northeast trending prospective 

tract that is delineated along a line of stratabound copper occurrences in northern Logar and southern 

Kabul Provinces (figs. 2A–11a, and 2A–12b). Prospecting in the Yagh-Darra Ghul-Darra copper-cobalt 
Chapter 2A. Summary of the Aynak Copper, Cobalt, and Chromium Area of Interest 67

subarea has taken place at the surface around the copper occurrences and includes some trenching 

around the Yagh-Darra occurrence (fig. 2A–25). The Ghuldarra I and II and Yagh-Darra occurrences 

were evaluated by Shcherbina and others (1975) and Kutkin and Gusev (1977). 

Figure 2A–19. Geology and mineral occurrences of the Kharuti-Dawrankehl copper-cobalt subarea. From 

Bohannon (2010b).
68 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

Figure 2A–20. General view looking southeast from the Kharuti II prospect toward the Khurdkabul and Chakari 

prospects in the Kharuti-Dawrankehl subarea. Photograph by Ted Theodore, U.S. Geological Survey. 

2A.3.6.3 Geology

The geology of the subarea (as mapped by Bohannon, 2010b) is dominated by a central mass of 

Weyalati Formation rocks and large masses of Neoproterozoic intrusive rocks that outcrop in the highest 

part of the subarea. The eastern and western flanks of the range, as well as most of the southern part of 

the subarea, are mapped as undifferentiated Weyalati and Loy Kwar Formations, suggesting that the 

dominant lithologies present should be amphibolite-facies schist, amphibolite, plagiogneisses, quartzites, 

and marbles of the Weyalati Formation and repetitive layers of dolomitic marble, carbonaceous quartz 

schist, and quartz-biotite-dolomite schist of the Loy Kwar Formation. Rocks of the Paleoproterozoic 

Sherdarwaza Formation are mapped along the northern margin of the subarea. In contrast to the other 

subareas, the Yagh-Darra Ghul-Darra subarea contains a prominent northwest trending series of 

elongated amphibolite intrusions of Neoproterozoic age that cut the Weyalati and Sherdarwaza 

Formations along the northern margin of the subarea; a quartz-rich intrusion of Cretaceous age is also 

present near the village of Gul Dara. A prominent normal fault of unknown vertical displacement or 

direction of throw bisects the subarea along an east-northeastly trend from the village of Gul Dara, 

passing just to the north of the Ghuldarra I occurrence (fig. 2A–24). 

2A.3.6.4 Known Deposits

No known deposits are present in the Yagh-Darra Ghul-Darra subarea.
Chapter 2A. Summary of the Aynak Copper, Cobalt, and Chromium Area of Interest 69

2A.3.6.5 Prospects and Anomalies

The Yagh-Darra Ghul-Darra subarea contains the Ghuldarra I and II, and Yagh-Darra 

occurrences. The Ghuldarra I occurrence is hosted in marble (thought to be of Vendian-Cambrian age by 

Shcherbina and others, 1975) in two zones containing disseminated covellite, chalcopyrite, chalcocite, 

and malachite. One zone is 1 km long and 15 to 35 m wide and the other is 450 m long and 10 to 80 m 

wide (Shcherbina and others, 1975; Abdullah and others, 1977). 

Figure 2A–21. Contact between intrusive meta-aplite and foliated dark amphibolite gneiss in the vicinity of the 

Kharuti II prospect in the Kharuti-Dawrankehl subarea. Photograph by Ted Theodore, U.S. Geological Survey. 

The Ghuldarra II occurrence consists of a copper mineralized zone 30 to 50 m long and 2 to 5 m 

wide hosted in a marble layer (thought to be of Vendian-Cambrian age by Shcherbina and others, 1975). 

The occurrence averages 0.55 percent copper (Shcherbina and others, 1975; Abdullah and others, 1977). 

The Yagh-Darra occurrence consists of an irregularly mineralized marble bed 20 to 50 m thick 

and more than 2 km long hosted in quartzite and micaceous garnet-amphibolite schist (thought to be of 

Vendian-Cambrian age by Shcherbina and others, 1975). One mineralized interval assayed 0.75 percent 

copper (Shcherbina and others, 1975; Abdullah and others, 1977). In 2009, a team of USGS geologists 

visited the area of the Yagh-Darra occurrence and reported their observations as follows: 

“Precambrian rocks of the Yagh-Darra locality are reportedly biotite-amphibole gneisses and 

migmatitic gneisses of Paleoproterozoic age. At Yagh-Darra the bedrock consists of steeply 

northwest-dipping amphibolite facies metaclastic rocks (marble, calc-silicate gneiss, 

muscovite-biotite schist, and quartzite) and lesser mafic and felsic gneisses (amphibolite and 
70 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

quartzofeldspathic gneiss) of probable volcanic origin (fig. 2A–26). None of the rocks show signs of 

partial melting; some of the metamafic gneisses formed pod-like boudins (100 m × 35 m) within 

quartzofeldspathic gneiss and schist. Few intrusive ingneous rocks were observed, except for a 

meta-aplite dike (5 m thick) sheared at its margins, that cut discordantly across the metamorphic 

layering (figs. 2A–27 and 2A–28). We saw little sign of copper mineralization at this locality. 

Where present, copper minerals consisted of rare green copper carbonates in marble and calc-silicate 

gneiss at or near the contact with mafic and felsic metavolcanic strata (fig. 2A–29). Although the 

area had many signs of quarry activity, only one had signs of copper mineralization. Quartzpotassium feldspar veins were observed at one locality (GPS 34.422261° N, 69.26019° E) but no 

signs of copper mineralization were evident.” 

2A.4 Metallogeny of Podiform Chromite Deposits

Podiform chromite deposits are lenticular-shaped, pod-like masses of massive coarse-grained to 

finely disseminated chromitite in the lowermost ultramafic parts of ophiolite complexes (Duke, 1983, 

1996; Albers, 1986; Singer and Page, 1986). Tabular, rod-shaped, and irregularly shaped bodies are also 

observed. They form in the lower part of the oceanic lithosphere as magmatic segregation deposits 

occurring in elongate pockets along spreading plate margins. They are subsequently preserved in 

collision zones when fragments of oceanic crust are scraped off into the mélange above subduction 

zones. They are, therefore, common features of accretion zones at continental margins and, along with 

their ophiolite host sequences, mark the closure of ocean basins between major crustal blocks.

Figure 2A–22. Isoclinally folded marble in the vicinity of the Kharuti II prospect in the Kharuti-Dawrankehl 

subarea. Photograph by Ted Theodore, U.S. Geological Survey. 

Rock types present in a complete ophiolite sequence consist of basal tectonized ultramafic rocks 

(mostly harzburgite), ultramafic cumulates (dunites and harzburgites), noncumulate and cumulate mafic 
Chapter 2A. Summary of the Aynak Copper, Cobalt, and Chromium Area of Interest 71

rocks (gabbros), a basaltic sheeted dike complex, pillowed basaltic lavas, and a covering of marine 

sedimentary rocks. The tectonites are thought to represent the residual, partially melted mantle, and the 

contact with the less deformed, layered ultramafic cumulates has been interpreted to represent the 

boundary between the mantle and the oceanic crust (the petrological Moho). Discordant bodies of dunite 

(and chromitite) are suggested to represent intrusions through the upper mantle and lower crust 

(Cawthorn and others, 2005). The chromite deposits are most common in the uppermost tectonized 

harzburgites and lower parts of ultramafic cumulates, which are commonly serpentinized. Most 

podiform chromite deposits worldwide are Phanerozoic in age with important examples in the 

Phillipines (Tertiary), Albania (Jurassic), Turkey (Paleozoic), and Kazakhstan (Paleozoic). A few 

Proterozoic examples are known in Egypt and Sudan (Duke, 1996). 

Figure 2A–23. Mica schist with near-vertical schistosity in the vicinity of the Kharuti II prospect in the KharutiDawrankehl subarea. Photograph by Ted Theodore, U.S. Geological Survey. 
72 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

Figure 2A–24. Geology and mineral occurrences of the Yagh-Darra Ghul-Darra copper-cobalt subarea. From Bohannon (2010b).
Chapter 2A. Summary of the Aynak Copper, Cobalt, and Chromium Area of Interest 73

Figure 2A–25. View looking north from the vicinity of the Yagh-Darra prospect. Photograph by Ted Theodore, 

U.S. Geological Survey. 

Figure 2A–26. Photograph showing inclined high-grade metamorphic rocks near the Yagh-Darra prospect. From 

bottom to top: marble and calc-silicate gneiss, amphibolite, and mica schist. Photograph by Ted Theodore, 

U.S. Geological Survey. 

Podiform chromite deposits are generally quite small with individual deposits ranging from a 

few tens to millions of metric tons with deposits greater than 1 Mt being rare. The largest known pod 

contains about 13 Mt of high-aluminum chromitite grading 36.5 percent Cr2O3. The largest mines 
74 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

generally exploit a number of pods with some mines producing from as many as 20 chromitite pods 

(Duke, 1996). In terms of dimensions, most podiform chromite bodies are the size of an autobus or a 

small building. A large deposit would be 100 to 200 m long, 50 m wide, and 10 m thick. 

Figure 2A–27. Photograph of meta-aplite felsic dike cutting across amphibolite (foreground) and mica schist 

(background). Photograph by Ted Theodore, U.S. Geological Survey. 

Figure 2A–28. Photograph of meta-aplite felsic dike (GPS 34.42783° N, 69.26404° E) cutting across amphibolite 

(foreground) and mica schist (background). Photograph by Ted Theodore, U.S. Geological Survey. 
Chapter 2A. Summary of the Aynak Copper, Cobalt, and Chromium Area of Interest 75

Chromite is the major ore mineral, which when in massive, near-monomineralic aggregates is 

referred to as the ore-rock chromitite. Ferrichromite, magnetite, ruthenium-osmium-iridium alloys, and 

the platinum group mineral laurite are possible accessory ore minerals. Gangue minerals in chromitite 

include olivine, orthopyroxene, clinopyroxene, and plagioclase. Secondary minerals include serpentine, 

chlorite, tremolite, talc, and carbonate. Chromitite displays a wide range of textures, from those clearly 

related to magmatic processes, to those produced during either brittle or ductile deformation. Layering is 

common and can be a result of cumulate textures, modal grading, and grain-size grading. Nodular 

textured chromite grains are a common and perhaps diagnostic feature of podiform chromite deposits 

and consist of loosely packed, ellipsoidal chromite nodules 5 to 20 mm in diameter in dunite matrix 

(Duke, 1996). Textures produced during deformation include lineation and foliation of chromite and 

olivine grains; stretching, boudinage, and fracturing of chromite grains; brecciation; and mylonitization. 

Chromite grains in massive chromitite tend to occur as coarse-grained (5 to 10 mm), interlocking 

anhedra.

Figure 2A–29. Photograph of an abandoned trench in the Yagh-Darra area showing secondary copper minerals 

(green) at the contact between calc-silicate gneiss (left) and quartzofeldspathic gneiss (felsic metavolcanics to the 

left. Photograph by Ted Theodore, U.S. Geological Survey. 

The chemical composition of chromite is variable, because chrome spinels form a solid solution 

having the general formula (Mg, Fe2+)(Cr, Al, Fe3+)2O4. Naturally occurring chromites have a wide 

range of chemical compositions that are indicative of the tectonic setting and, therefore, of the deposit 

subtype. Chromite from podiform deposits are low in Fe3+ and TiO2, and the major compositional 

variation is in the amount of chromium-aluminum substitution. The Mg:(Mg+Fe2+) ratio in chromite 

from podiform chromite deposits does not vary greatly but does show a slight negative correlation with 

the Cr:(Cr+Al) ratio. Systematic variation of chromite compositions across individual deposits has been 

observed in some deposits and includes the upward decrease in the Cr:Fe ratio in a single lens. A 

significant increase of Cr:Fe and Cr:(Cr+Al) with increasing depth below the petrologic Moho has also 

been documented (Duke, 1983). Podiform chromite deposits are highly resistant to weathering and 

oxidation. However, despite this characteristic the discovery of a significant number of PGE-bearing 
76 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

podiform chromite deposits has been preceeded by the discovery and exploitation of PGE placer 

deposits downstream of the podiform chromite deposits. 

Two podiform chromite grade and tonnage models have been produced. The major podiform 

chromite deposit model was built using data from 174 deposits from around the world (Singer and 

others, 1986). Major podiform chromite deposits have a mean tonnage of 20,000 t with 80 percent of the 

deposits ranging from 2,200 to 200,000 t; 80 percent of the grades range from 33 percent to 52 percent 

chromite; the mean is 46 percent (Singer and others, 1986). Figure 2A–30 shows the major podiform 

tonnage model with the estimated tonnages of six known Afghanistan chromite deposits superimposed 

(Volin, 1950). The other grade and tonnage model, minor podiform chromite deposits, does not apply to 

the Logar Ophiolite Complex (LOC). 

2A.4.1 Ultramafic-Hosted Talc-Magnesite

Talc and magnesite are two magnesium-rich minerals that may occur in the same or spatially 

associated deposits; this includes deposits hosted by ultramafic rocks. The term “talc” is a mineral name, 

but it is also commonly used to describe rocks that contain the mineral in variable amounts. Massive 

talcose rock is called steatite, and an impure massive variety is known as soapstone (Virta, 2007). The 

mineral talc is extremely soft with a Mohs hardness of 1 (as compared to diamond with a hardness of 

10.) Talc, which is most familiar to people as talcum powder, but has many other uses, is a hydrous 

silicate mineral with the chemical formula Mg3Si4O10(OH)2. Although talc is commonly relatively pure 

in composition, small amounts of aluminum, iron, manganese, and titanium may be present as 

impurities. Talc can be translucent white, apple green, dark green, or brown, depending on the 

composition of these impurities. Structurally, talc consists of microscopic platelets. The bonds holding 

these platelets together are very weak, which enable the platelets to slide by one another and result in the 

greasy feel of talc (U.S. Geological Survey, 2000).

Magnesite (MgCO3) is the dominant industrial mineral source for magnesia (MgO). Magnesia is 

characterized by its inertness and high melting point and is commonly used to produce high-temperature 

refractories, chemicals and fertilizer, and magnesium—the lightest of the structural metals (Bodenlos 

and Thayer, 1973; Harben and Kužvart, 1996a; Kramer, 2001). Most magnesite and magnesia extracted 

from brines and seawater are processed into dead-burned magnesia (calcined at a temperature exceeding 

1,450°C) or caustic-calcined magnesia (calcined at a lower temperature that leaves a small amount of 

CO2 in the resulting compound). Dead-burned magnesia is used predominantly for refractories, whereas

caustic-calcined magnesia is the preferred starting material for chemicals, cement, filler, fertilizers, and 

many other uses (Harben and Kuzvart, 1996a). 

Health concerns have been expressed about the association of asbestos with talc

(http://www.natural-health-information-centre.com/talc.html) The alteration of serpentinite by siliconrich fluids may produce chrysotile asbestos as well as talc. In addition, tremolite amphibole (which can 

be asbestiform) may be an intermediate product of carbonation of serpentinite. Chrysotile forms at a 

lower temperature than talc and differs in some other formational conditions, so although chrysotile is 

chemically similar to talc, it is unlikely that it will be present within the part of a talc deposit that has a 

grade suitable for mining. Overall, most talc is asbestos free. The general public is in contact with talc in 

powders and its potential for inhalation has drawn the attention of health researchers. In mining and 

processing talc, miners, and factory workers may be at a greater risk because of prolonged exposure to 

fine particles of talc. When talc is being mined and processed, large amounts of dust particles may be in 

the air and workers could inhale it into their lungs. When massive concentrations are inhaled, long-term 

accumulation may occur in the lungs, and too much inhalation may cause lung disease and other health 

problems (http://www.knowabouthealth.com/talc-powder-can-pose-severe-health-risk/2362/). Talc has 

not been proven to cause human lung cancer, even in mine and factory workers. Research shows talc 

miners have the same mortality rate as nontalc miners with regard to lung cancer.
Chapter 2A. Summary of the Aynak Copper, Cobalt, and Chromium Area of Interest 77

There have been numerous attempts to develop descriptive models of ultramafic-hosted 

magnesite, talc, and talc-magnesite mineral deposits (Paradis and Simandl, 1996; Page 1998a,b; Simandl 

and Ogden, 1999). Talc and magnesite are commonly found together, but also separately as 

replacements for serpentinite. Asbestos deposits, magnesite deposits, and podiform chromite deposits 

are commonly associated deposits, as are “verde antique” dimension stone deposits (Page, 1998a,b; 

Simandl and Ogden, 1999). The following description draws from the previously referenced deposit 

models as well as other sources.

Magnesite, talc, and mixed talc-magnesite deposits occur in serpentinized zones within 

ultramafic rocks in tectonically transported rocks and greenstone belts, which may or may not have an 

ophiolite affiliation (Simandl and Ogden, 1999). Deposits are commonly associated with large faults or 

shear zones. Serpentinites that contain these deposits have undergone additional carbonation and 

alteration by hydrothermal fluids containing a significant amount of carbon dioxide (Pohl, 1990, 

McCarthy and others, 2006). Whether talc and (or) magnesite forms from this process is a function of 

the carbon dioxide and magnesium content of the altering hydrothermal fluids, the original magnesium

content of the host rock, the completeness of the alteration process, and the spatial relationship of the 

alteration to regional faults and siliceous country rocks (Koons, 1981; Harben and Kužvart, 1996a,b; 

Simandl and Ogden, 1999). In progressive carbonation of serpentinite, talc-magnesite mineralization 

will be followed by quartz-magnesite and magnesite. Talc content may also result or be enhanced from 

steatization of talc-carbonate rock by subsequent Silicon-rich fluids or from the metamorphic reaction of 

serpentinite and talc-carbonate rock with siliceous country rock (Harben and Kužvart, 1996b; McCarthy 

and others, 2006). 

Ultramafic magnesite deposits are commonly small compared to other deposits of magnesite, 

although the size range of the deposits is quite variable. Deposits consist of cryptocrystalline magnesite 

in the form of veins, nodules, stockworks, and lenses in altered serpentinite (Page, 1998b; Kramer, 

2001). Deposits related to regional fault systems cutting through ultramafic rocks are commonly 

magnesite rich (Simandl and Ogden, 1999). 

Ultramafic talc deposits are the most abundant type of talc deposits, although the majority of 

world production of talc is from metasedimentary deposits (McCarthy and others, 2006). In place of 

magnesium within its crystal lattice, talc from serpentinite-hosted deposits may contain significant levels 

of iron, nickel, and (or) chromium that affect the color of the talc and cannot be removed. Talc grades 

are commonly higher near the periphery of the ore bodies where steatization may have been more 

pronounced (Harben and Kužvart, 1996b; McCarthy and others, 2006).

Whether or not a deposit will contain talc or magnesite, or some unknown combination of the 

two, can be extremely difficult or impossible to predict, especially in the absence of detailed geologic 

information. No studies of the Afghanistan ultramafic rocks and their serpentinization are available that 

would allow scientists to discern whether talc or magnesite could be the dominant magnesium mineral. 

Ultramafic talc and magnesite deposits may be spatially associated with chrysotile asbestos, podiform 

chromite, nickel laterite, and “verde antique” dimension stone deposits in related rocks (Page, 1998a,b; 

Simandl and Ogden, 1999). Known occurrences in Afghanistan indicate that only talc with spatially 

associated asbestos has been definitively identified in the ultramafic rocks; the known magnesitedominated deposits are believed to be a different deposit type. Grade and tonnage modeling indicates 

that there is a continuum between talc-only and magnesite-only deposits within serpentinized ultramafic 

rocks, but grade and tonnage models were constructed separately for talc and magnesite, as many 

deposits contain only one of the commodities in significant amounts. Magnesite may occur with or 

without talc in the ultramafic rocks. Therefore, the tracts should be considered permissive for both talc 

and magnesite, although known occurrences do not contain magnesite and, in the absence of better 

information, would suggest that magnesite is unlikely to occur in significant amounts in these rocks. 

Ultramafic-hosted talc-magnesite deposits commonly correspond to aeromagnetic lows; 

unserpentinized parts of ultramafic host rocks present strong magnetic anomalies (Simandl and Ogden, 

1999). Deposits are commonly found near contacts with country rocks and in, or near, faults and 
78 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

fractures, as well as spatially associated with podiform chromite and serpentine-hosted asbestos deposits 

(Page, 1998a,b). Deposits may be relatively resistant to weathering and may accumulate as residue 

above and near buried talc bodies (Blount and others, 1995; Page, 1998b) or form topographic lows that 

can be covered by lakes and swamps (Simandl and Ogden, 1999). 

Figure 2A–30. Graph showing estimated tonnages of Afghan podiform chromite occurrences plotted on the major 

podiform chromite tonnage curve (from Peters and others, 2007, after Singer and others, 1986).

2A.4.2 Serpentine-Hosted Asbestos

The commercial term "asbestos" is applied to a group of six fibrous (large length-to-width ratio) 

silicate minerals amenable to mechanical separation into fine filaments of considerable tensile strength 

and flexibility. These minerals are essential to modern technology in certain relatively low-volume uses 

by virtue of their unique combinations of physical and chemical properties (Shride, 1973; Jensen and 

Bateman, 1981). 

These fibrous minerals share several properties which qualify them as asbestiform fibers: 

(1) they are found in bundles of fibers which can be easily separated from the host matrix or cleaved into 

thinner fibers; (2) the fibers exhibit high tensile strengths and show high length, such as their diameter 

(aspect) ratios that range from a minimum of 20 up to greater than 1,000; (3) they are sufficiently 

flexible to be spun; and (4) macroscopically, they resemble organic fibers, such as cellulose (Virta, 

2002). 
Chapter 2A. Summary of the Aynak Copper, Cobalt, and Chromium Area of Interest 79

Properties that are used to evaluate asbestos as to its ultimate use are flexibility, length of fiber, 

tensile strength, and chemical reactivity, in addition to resistance to heat, electrical conductance, and 

filtration characteristics (Shride, 1973). Uses for asbestos include roofing products, gaskets, and friction 

materials. Asbestos was once used in automobile brake pads and shoes, but since the mid-1990s, most 

brake linings are now asbestos free. The resistance of asbestos to fire has long been exploited for a 

variety of purposes. In ancient Egypt, asbestos was used in fabrics used as burial cloths. Nearly all 

asbestos produced worldwide is chrysotile (Virta, 2002). In 2005, world production increased to 2.40 Mt

from 2.36 Mt that was produced in 2004 (Virta, 2007).

Asbestos minerals, which differ in chemical composition and physical properties, fall into two 

broad groups—serpentine and amphibole. The serpentine group consists of the mineral chrysotile, 

traditionally the most valuable variety of asbestos and produced in the greatest quantity. The amphibole 

group includes anthophyllite, crocidolite, amosite, tremolite, and actinolite (Jensen and Bateman, 1981). 

Riebeckite (known under the variety name crocidolite) and amosite make up much of the remaining 

production, with very minor production of anthophyllite, tremolite, and actinolite (Shride, 1973). 

Chrysotile or "white asbestos" has fine fibers that can be spun into as much as 4.35 km of thread 

per kilogram. Some varieties withstand 2,750°C (Jensen and Bateman, 1981). Chrysotile asbestos occurs 

in two geologic settings, (1) from stockworks of veins in serpentinized peridotite, pyroxenite, and dunite 

(ultramafic-hosted asbestos); and (2) from veins confined to thin serpentine layers in limestone and other 

carbonate rocks. This assessment of asbestos resources in Afghanistan deals exclusively with ultramafichosted chrysotile deposits. Chrysotile is less harmful than the other types of asbestos since it is less 

friable, and therefore less inhalable. 

Crocidolite or "blue asbestos" comes chiefly from South Africa where it occurs as a long, coarse, 

flexible spinning fiber with low fusibility and high resistance to acids (Jensen and Bateman, 1981). 

Anthophyllite occurs as mass fiber, and is a short, brittle, nonspinning fiber used mostly in insulation. 

Amosite is an iron-rich variety of asbestos that occurs in long splintery, coarse fibers, some of which can 

be spun. Amosite is chiefly used as a binder for heat insulators (Jensen and Bateman, 1981). Tremolite 

and actinolite have little commercial value.

Chrysotile asbestos deposits occur as chrysotile asbestos in stockworks and veins in 

serpentinized ultramafic rocks that consist of harzburgite, dunite, wehrlite, and pyroxenite (Duke, 1984; 

Page, 1986; Hora, 1997; Obolenskiy and others, 2003). Serpentinites may be part of an ophiolite 

sequence in unstable accreted oceanic terranes, within Alpine-type ultramafic rocks, or in synvolcanic 

intrusions of komatiitic affinity in Archean greenstone belts. 

The serpentinite host rocks must have a nonfoliated texture and must be located near a fault that 

was active during a change in orientation of the regional stress field (Hora, 1997). Subsequent 

deformation and igneous intrusion may be important. The serpentinized ultramafic rocks are highly 

fractured and veined and may be intruded by pegmatite dikes (Obolenskiy and others, 2003). White 

chrysotile asbestos replaces massive ultramafic and serpentinized ultramafic bodies and fills fractures

that developed in shear zones near contacts between serpentinized bodies and igneous rocks that were

emplaced into serpentinite (Wrucke, 1995). Associated minerals include magnetite, brucite, talc, and 

actinolite-tremolite (Page, 1986). 

Orris (1986) modeled the grades and tonnages of 50 serpentine-hosted asbestos deposits and 

determined that 80 percent have between 2.7 and 8.0 percent asbestos and from 4.6 to 150 Mt of 

material. The mean grade and tonnage are 4.6 percent asbestos and 26 Mt. 
80 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

2A.4.3 Economic Geology

2A.4.4 Characteristics of the Logar Podiform Chromite Deposits

The characteristics of the podiform chromite deposits in the Aynak AOI are best exemplified by 

features of the Logar deposits. Maps of some of the known podiform chromite deposits in Logar Valley 

are included in figures 2A–31 through 2A–39. The major host-rock types are serpentinized harzburgite 

and dunite with minor noritic dikes in the southernmost part of the LOC. These rock types were noted 

but not mapped by Volin (1950). Chromite deposits are predominantly found in envelopes of dunite 

surrounded by harzburgite, typical of chromite occurrences in ophiolites, and also in association with 

kilometer-sized bodies of lherzolite and cross-cutting orthopyroxenite dikes (Benham and others, 2009). 

Most of the deposits are relatively small with dips between 32 and 45 degrees toward the southwest. The 

largest body (Logar #5) consists of two lenses, one 97.5 m long and 10 m wide, and a second 65 m long 

and up to 5 m wide (figs. 2A–34 through 2A–36). The margins of all the chromite bodies are sharp and 

irregular, and the immediate wallrocks are generally serpentinized and have developed close-spaced 

planar fabric and fracturing parallel to the contacts (Benham and others, 2009). 

Figure 2A–31. Vertical cross section of chromite deposit number 1 in the Logar Valley, Afghanistan. From Volin 

(1950). 

Two small chromite quarries visited by the British Geological Survey in 2006 (Benham and 

others, 2009) are described as containing massive chromitite, areas of disseminated mineralization with 

occasional blebs of chromite associated with 1- to 2-cm thick carbonate veins and, less commonly, 

submassive chromitite. Petrographic study of chromitites indicates the presence of 5 to 10 percent 

interstitial silicate minerals in the ultramafic lithologies, most of which is olivine with minor alteration 

to serpentine. More thoroughly altered samples contain mostly serpentine and chlorite with remnant 
Chapter 2A. Summary of the Aynak Copper, Cobalt, and Chromium Area of Interest 81

olivine. Chromite grains are generally fresh with red to red-brown margins and minor darkening along 

fractures. Altered samples show alteration of chromite to ferrit-chromite and magnetite. Some samples 

contain thin carbonate veinlets (Benham and others, 2009). 

Platinum group minerals (PGM) were found in two samples. One sample consisted of an

8-micron-sized grain of native platinum with minor iron that was present in a dunite sample associated 

with fine-grained serpentinization of olivine; the second sample contained a 10-micrometer-size grain of 

ruthenium-iridium alloy along a chromium spinel-chlorite grain boundary. The presence of PGM, in 

association with alteration minerals serpentinite and chlorite, indicates possible remobilization of these 

minerals during alteration of the host rocks (Benham and others, 2009).

Figure 2A–32. Map view and cross sections of chromite deposit number 2 in the Logar Valley, Afghanistan (Volin, 

1950).

2A.4.5 Logar Valley Chromite Subarea

2A.4.5.1 Location

The Logar Valley chromite subarea is located in the northern part of Logar Valley in 

northeastern Afghanistan starting 33 km south of Kabul and extending 15.5 km southward into the 

valley in the Muhammad Agh, Chahar Asyab, Maydan Shahr, Nirkh, and Puli alam Districts of Kabul 

and Logar Provinces. The Logar River traverses the valley south to north before it joins the Kabul River 

east of Kabul. The occurrences are mostly clustered in two groups about 9 km apart in the hills on the 

western side of the valley, and all are easily accessible from the Kabul-Gardez road located next to the 

Logar River (figs. 2A–5 and 2A–6). A northern cluster of deposits is located about 7 km northwest of 

the village of Muhammad Agha, and a southern cluster is located to the southwest of Dewalak about 5 

km south of Muhammad Agha (Benham and others, 2009). 
82 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

2A.4.5.2 Exploration History

Chromite occurrences are present in the Logar Valley and delineate a 45-km-long section mostly 

along the western flank of the valley with the northernmost occurrence about 14 km south of Kabul 

(figs. 2A–4, and 2A–6). Chromite mineralization in the area was first recognized by the U. S. Bureau of 

Mines in 1949–1950 (Volin, 1950). Volin (1950) documented 10 surface outcrops of chromite, 

numbered 1–10, occurring as massive lenses, pods, and irregular-shaped bodies of massive chromitite, 

predominantly hosted within small dunite pods in harzburgite (Siebdrat, 1971). Four of the areas (1, 2, 3, 

and 5) contain 27 diamond-drill holes totaling 975.7 m. The other areas were sampled by a combination 

of jack-hammer holes, channel sampling, and trenching. Details of the results of the work can be found 

in Volin (1950). 

Figure 2A–33. Vertical cross sections of chromite deposit number 2 in the Logar Valley, Afghanistan (Volin, 

1950).

Additional surveys in the region during the 1970s by Soviet and Afghan geologists identified 

copper, chromite, beryl, mica, graphite, and asbestos occurrences in the region; however, the additional 

chromite bodies in the LOC were reported to be isolated lenses a few meters in size and, therefore, not 

economically important (Denikaev and others, 1971; Nevretdinov and Mirzamon, 1979; Benham and 

others, 2009). 

Additional work by the (German) Federal Institute for Soil Research identified 18 lenticularshaped chromite bodies, including some of those previously identified by the U.S. Bureau of Mines 

(USBM) (Siebdrat, 1965; 1971; Benham and others, 2009). The main sources of information concerning 

the chromite deposits in the Logar Valley are Volin (1950), Siebdrat (1965; 1971), and Benham and 

others (2009). In a review of previous work in the LOC, Benham and others (2009) state that kilometersized bodies of lherzolite (and, later, cross-cutting orthopyroxenite dikes) are also commonly associated 

with outcrops of chromite. This study is consistent with Siebdrat’s work (1965; 1971) wherein chromite 
Chapter 2A. Summary of the Aynak Copper, Cobalt, and Chromium Area of Interest 83

is associated with harzburgite and dunite. Benham and others (2009) concluded that the observed 

association of rock types represent the upper part of the mantle sequence close to the mantle transition 

zone. Volin (1950) and his crew carried out mapping, drilling, channel sampling, and chemical analyses 

on the chromite deposits in the region. The ultramafic-mafic rocks that host these deposits in 

Afghanistan are part of a series of ophiolites emplaced during the Eocene that extend from Afghanistan 

and western Pakistan through the Arabian Peninsula (Gnos and others, 1997). 

Figure 2A–34. Map view of chromite deposit number 5 in the Logar Valley, Afghanistan (Volin, 1950).

2A.4.5.3 Geology

The major rock types are serpentinized harzburgite and dunite with minor noritic dikes in the 

southernmost areas. These rock types were noted but not mapped by Volin (1950). The chromite 

deposits are all found in envelopes of dunite surrounded by harzburgite, typical of chromite occurrences 

in ophiolites. 

2A.4.5.4 Known Deposits

The Logar deposits (figs. 2A–6, 2A–31 through 2A–36) are located about 8 km west of the 

Logar River on the southern flank of Qatarsang where they occur as two parallel lenticular chromite 

zones. The zones strike northwest, are 10 to 100 m long and 1 to 10 m thick, and predominantly consist 

of chromite in the middle of a large Eocene ultrabasic intrusive. The three largest deposits (1, 2, and 5) 

are collectively referred to by Abdullah and others (1977) as the Logar chromite deposit. The drilling 

investigations at these three deposits—and projection of the smaller deposits to a depth of 8 m (an 

arbitrary but reasonable estimate)—yielded a resource estimate of 181,200 tons containing 35.8 to 

57.5 percent Cr2O3. Of this, about 15 percent (27,000 tons) is high-grade metallurgical chromite with 

55.9 percent Cr2O3 and a Cr:Fe ratio of 3.5:1. The remaining resource contains less than 45 percent 

Cr2O3 and high levels of Al2O3 (Benham and others, 2009). The three largest deposits (the Logar 

chromite deposit) make up 92 percent of the total and of these, only two contained high-grade ore. Later 
84 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

work by Siebdrat (1965; 1971) increased the resource estimates to about 3 million tons of “visible or 

probable” ore and an additional 200,000 tons as “possible,” although it is unclear what reporting 

standard was used or whether these additional resources were based upon new drilling or geophysical 

data. Little chromite is reported to remain at the surface in these deposits, as most of the chromite has 

been removed by quarrying (Benham and others, 2009). 

Figure 2A–35. Map view and cross sections of chromite deposit number 5 in the Logar Valley, Afghanistan 

(Volin, 1950).

2A.4.5.5 Prospects and Anomalies

The Werek chromite occurrence is located on the curving eastern flank of Tor Werek Ghar 

(fig. 2A–6). The occurrence grades 37.3 percent Cr2O3 

The Makhmudgazi 1 occurrence (fig. 2A–6), located on the northern slope of Kohe 

Saydmahmude Ghazi about 2 km west of the Logar River, consists of two massive chromite occurrences 

that are 5 by 40 m and 3 by 50 m, as well as a number of small lenses in Eocene ultrabasic rocks. Volin 

(1950) estimated resources to be 5,600 tons grading 43.4 percent Cr

and occurs as a 29-m by 3-m-thick body in an 

Eocene ultrabasic plug (Shcherbina and others, 1975). No estimate of resources is known. 

2O3

The Makhmudgazi 2 occurrence (fig. 2A–6) is situated about 1 km south of Makhmudgazi 1 in 

an Eocene peridotite. This occurrence consists of a number of chromite lenses ranging from 1 by 5 m to 

2 by 51 m. Volin (1950) reports the resources to total 1,300 ton grading 43.4 percent Cr

. 

2O3

Makhmudgazi 3 occurs on the northern slope of Kohe Saydmahmude Ghazi about 3 km west of 

the Logar River. Two massive chromite occurrences, each between 30 and 40 m long and 0.3 and 0.5 m 

thick occur in Eocene ultrabasic rocks (fig. 2A–6). Resources were estimated in 1950 to be 840 tons 

grading 42.3 percent Cr

. 

2O3 

At Koh-i-Kalawur, along the southeast foot of Kohe Saymahmude Ghazi east of the Logar River, 

seven chromite lenses as large as 4.5 by 27 m are hosted in an Eocene ultrabasic plug (fig. 2A–40).

Resources were estimated to be 4,300 tons grading 42.8 percent Cr

(Volin, 1950). 

2O3 (Volin, 1950). This occurrence 
Chapter 2A. Summary of the Aynak Copper, Cobalt, and Chromium Area of Interest 85

may be, or is located near, the Kulangar No. 10 chromite occurrence reported by Bowersox and 

Chamberlin (1995). 

Figure 2A–36. Three dimensional representation of ore blocks in chromite deposit number 5 in the Logar Valley, 

Afghanistan (Volin, 1950).

Volin (1950) reports an unnamed chromite showing at 34°16'20" N, 68°53'10" E, which is on the 

western flank of Sro Ghar and south of the merger of the Kabul River and a river from the northwest. 

Chromite float is seen in eluvial talus covering an area of 30 by 20 m that is derived from an Eocene 

peridotite (Volin, 1950). No estimate of resources was reported.

Another unnamed chromite showing is also reported at 34°14'10" N, 68°52'20" E, which is on 

the western flank of the mountains between Sro Ghar and Tor Ghar. Several chromite lenses are present 

up to 6 to 20 m long and as much as 10 m thick in Eocene ultrabasic intrusive rocks (Volin, 1950). No 

estimate of resources was made by Volin.

A third unnamed chromite showing can be found at 34°08'50" N, 68°58'05" E. A chromite lens 

about 10 m long and 2 m thick occurs in Eocene ultrabasic intrusive rocks at this site (Volin, 1950). 

Resources are estimated at 200 tons grading 44.1 percent Cr2O3

A cluster of asbestos deposits and occurrences is centered about 35 to 45 km south to southwest 

of Kabul. The Logar asbestos deposit in Logar Province consists of asbestos in serpentinized zones in 

fault zones along the contact of porphyry and lamprophyre dikes in Eocene peridotite. Chrysotile occurs 

in stockworks of variable size in serpentinized zones that are a few tens of meters to 600 m long and as 

much as 5 or 6 m thick. The stockworks consist of thin veinlets containing 0.8 to 9.0 percent asbestos 

fiber (United Nations Economic and Social Commission for Asia and the Pacific, 1995). 

. 
86 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

Figure 2A–37.

The Spinkala asbestos occurrence is present in Eocene peridotite in a serpentinized zone that is 

50 to 700 m wide with predominant slip-fiber asbestos and minor cross-fiber asbestos. The occurrence 

grades 0.25 to 7.88 percent chrysotile asbestos (Shcherbina and others, 1975). Cross-fiber asbestos at the 

Kohe Moghu Aba occurrence is found in a 300 m long by 20 to 50 m thick zone along diabase dikes in 

Eocene serpentinite. The mineralized zone grades 3.83 percent asbestos (Shcherbina and others, 1975). 

Map view of chromite deposit number 6 in the Logar Valley, Afghanistan (Volin, 1950).

The Abparan asbestos occurrence has been identified as an asbestos-bearing zone in a 

500-m-long Eocene peridotite zone. The mineralized zone is about 300 m long and 5 to 20 m wide with 

asbestos in veinlets 1 to 15 mm thick (Shcherbina and others, 1975). 

The Waghjan asbestos occurrence is found in Eocene peridotite along a 500-m-long zone where 

lenticular asbestos-bearing bodies 30 to 80 m long and 0.3 to 3.0 m thick have cross-fiber veinlets 0.5 to 

5.0 mm thick (Shcherbina and others, 1975). 

At the Shakhsi asbestos occurrence, strongly serpentinized asbestos-bearing zones 30 to 200 m 

long and 0.3 to 6 m thick occur along faults in Eocene peridotite. These mineralized zones carry as much 

as 9.5 percent chrysotile asbestos with an average of 0.8 percent asbestos (Shcherbina and others, 1975) 

(fig. 2A–40). 

Four additional asbestos showings are present in Logar Province. At the first showing, crossfiber asbestos veinlets having fibers 4 to 5 mm long are found in a serpentinized zone 150 to 200 m long 

and 20 to 30 m wide in Eocene ultramafic rocks (Shcherbina and others, 1975). The second showing 

occurs as serpentinized zones in Eocene peridotite. The zones are a few tenths of meters long and 0.3 to 

0.5 m thick with cross-fiber asbestos in veinlets (Shcherbina and others, 1975). The third showing 

consists of serpentinite zones as much as 30 m long and 0.1 to 1.0 m thick in Eocene peridotite. The 

zones carry cross-fiber asbestos in veinlets 2 to 5 mm thick (Shcherbina and others, 1975). The last 

reported asbestos showing in Logar Province is located mainly along the contact between diorite-gabbro 

and Eocene peridotite where a zone 1,200 m long and 100 to 200 m thick contains chrysotile asbestos 

veinlets having fibers 1.5 to 2 mm long (Shcherbina and others, 1975). 

The Lalandar talc-magnesite occurrence is located close to the contact between small Eocene 

ultramafic bodies and interbedded slate and marbled limestone of Late Permian age. The occurrence 
Chapter 2A. Summary of the Aynak Copper, Cobalt, and Chromium Area of Interest 87

consists of four pervasive talc-bearing zones 100 to 800 m long with 20 by 30 m nests and lenses of talc. 

These occurrences have been exploited by local residents (Shcherbina and others, 1975) and may or may

not be of the ultramafic type.

Figure 2A–38. Map view of chromite deposit number 9 in the Logar Valley, Afghanistan (Volin, 1950).

Figure 2A–39. Map view of chromite deposit number 10 in the Logar Valley, Afghanistan (Volin, 1950).
88 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

Figure 2A–40. Locations of chromite occurrences in the Logar Ophiolite Complex. Imagery base map, 90 m 

shaded DEM from Peters and others (2007).

2A.5 Summary of Potential

Sediment-hosted copper deposits are large, relatively low grade deposits that may also contain 

significant amounts of cobalt, silver, uranium and, less commonly, gold and platinum group elements as 

byproducts. The extraction of these deposits would require hundreds of million dollars in capital 

investment (http://www.newsecuritybeat.org/2010/03/copper-in-afghanistan-chinese.html) and also 

require significant resources of operational power and transportation infrastructure. Development from 

discovery to production may take up to 10 or more years. The deposits commonly are mined by large 

open-pit mines, but especially rich deposits may also be mined by underground methods. Sedimenthosted copper deposits are commonly associated with a number of other deposit types, such as halite, 

potash, gypsum, and anhydrite deposits, which occur in the same sedimentary sequences. Sandstone 

uranium, unconformity uranium, and Kipushi-type copper-lead-zinc deposits can occur in the same 

districts. In addition, the iron oxide copper-gold and basaltic copper deposit submodels may be 

applicable within some of the areas that were studied.

In light of the presence of the world-class Aynak copper-cobalt deposit and a number of smaller 

deposits with reported resources, the future potential for discovery of additional copper-cobalt deposits 

in the Aynak area of interest and subareas is regarded as high. 

Podiform chromite deposits are generally very small deposits that are not economically feasible 

to extract unless significantly large numbers are present such that sufficient tonnages in aggregate can be 

achieved. Some podiform chromite deposits contain platinum group elements as byproducts, which can 

represent significantly enhanced economic value. These deposits occur in the ultramafic parts of 
Chapter 2A. Summary of the Aynak Copper, Cobalt, and Chromium Area of Interest 89

ophiolite sequences that are also host to industrial mineral deposits of talc-magnesite and asbestos. The 

mining of asbestos, however, can have undesirable environmental consequences which decreases the 

likelihood of exploitation. Although the future potential for additional discovery and exploitation of 

chromite deposits in the Logar Valley is regarded as low, chromite deposits may be suitable for artisanal 

mining and direct transport of chromite ore to smelters.

2A.6 References Cited

Abdullah, S., Chmyriov, V.M., Stazhilo–Alekseyev, K.F., Dronov, V.I., Gannan, P.J., Rossovskiy, L.N., 

Kafarskiy, A.Kh., and Malyarov, E.P., 1977, Mineral resources of Afghanistan (2d ed.): Kabul, 

Afghanistan, Republic of Afghanistan Geological and Mineral Survey, 419 p. 

Abdullah, S., Chmiriov, V.M., Stazhilo-Alekseev, K.F., Dronov, V.I., Kofarsky, A.K., and Malyarov, 

E.P., 1977, Mineral resources of Afghanistan: Republic of Afghanistan, Ministry of Mines and 

Industries, Afghan Geological and Mines Survey, 419 p. 

Afghanistan Geological Survey, 2006a, The Aynak copper deposit: Afghanistan Geological Survey, 

accessed September 1, 2006, at http://www.bgs.ac.uk/afghanminerals/mininfo.htm. 

Afghanistan Geological Survey, 2006b, The potential for copper: Afghanistan Geological Survey, 

accessed September 1, 2006, at http://www.bgs.ac.uk/afghanminerals/mininfo.htm. 

Akhmadi, A.K., 1992, Gradiyentno–vektornyye kharakteristiki zonal'nosti Osnovnoy rudnoy zalezhi 

Zapadnogo uchastka mestorozhdeniya Aynak v Afganistane [Gradient and vector characteristics of the 

main Aynak ore deposit in Afghanistan]: Otechestvennaya Geologiya, v. 1992, no. 8, p. 30–36. 

Akocdzhanyan, L.A., Kryukov, Ye.A., Zagorodniy, G.G., Kashin, A.A., Koloskov, V.P., Kubatkin, 

L.V., Makimov, T.M., Nevretdinov, E.B., Novosolcev, V.M., Sulikayev, K.I., Cvetkov, L.P., 1977, 

Preliminary report on results of geological exploration of Aynak copper deposit in 1974–1976: Kabul, 

Afghanistan, Geological Survey Archive, vol. 1–9 and sup. vol. 1–3. [In Russian.] 

Albers, J.P., 1986, Descriptive model of podiform chromite, in Cox, D.P., and Singer, D.A., eds., 

Mineral deposit models: U.S. Geological Survey Bulletin 1693, p. 34. 

Avila-Salinas, W., 1990, Origin of the copper ore at Corocoro, Bolivia, in Fontbote, Amstutz, G.C., 

Cardozo, M., Cedillos, E., and Frutas, J., eds., Stratabound ore deposits of the Andes: BerlinHeidelberg, Springer Verlag, p. 659–670. 

Benham, A.J., Kovac, P., Petterson, M.G., Rojkovic, I., Styles, M.T., Gunn, A.G., McKervey, J.A., and 

Wasy, A., 2009, Chromite and PGE in the Logar ophiolite complex, Afghanistan: Applied Earth 

Science (Trans. Inst. Min. Metall. B), v. 118, no. 2, p. 45–58. 

Blount, A.M., Lathrop, R.G., and Parkinson, G.A., 1995, Application of x-ray diffraction and visiblenear infrared spectroscopy in talc exploration, in Simard, C.M., comp., and Walker, B.J., ed., 

Proceedings, 28th Forum on the Geology of Industrial Minerals: West Virginia Geological and 

Economic Survey and U.S. Bureau of Mines Circular C–46, p. 50–55. 

Bodenlos, A.J., and Thayer, T.P., 1973, Magnesian refractories, in Brobst, D.A., and Pratt, W.P., eds., 

United States Mineral Resources: U.S. Geological Survey Professional Paper 820, p. 379–384. 

Bohannon, R.G., 2010a, Geologic and topographic maps of the Kabul north 30′ × 60′ quadrangle, 

Afghanistan: U.S. Geological Survey Scientific Investigations Map 3120, 34 p., 2 map sheets, scale 

1:100,000, available at http://pubs.usgs.gov/sim/3120. 

Bohannon, R.G., 2010b, Geologic and topographic maps of the Kabul south 30′ × 60′ quadrangle, 

Afghanistan: U.S. Geological Survey Scientific Investigations Map 3137, 34 p., 2 map sheets, scale 

1:100,000, available at http://pubs.usgs.gov/sim/3137. 

Bowersox, G.W., and Chamberlin, B.E., 1995, Gemstones of Afghanistan: Tucson, Arizona, Geoscience 

Press, 220 p. 

British Geological Survey, 2005a, Aynak information package, in Afghanistan Geological Survey and 

the British Geological Survey, comps., Part I, Introduction: Kabul, Afghanistan, Ministry of Mines, 

Department of Mines Affairs, available at 

http://www.bgs.ac.uk/afghanminerals/DMA_tender_docs.htm. 
90 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

British Geological Survey, 2005b, Aynak information package package, in Afghanistan Geological 

Survey and the British Geological Survey, comps., Part II, Geological setting of Aynak and summary 

of exploration: Kabul, Afghanistan, Ministry of Mines, Department of Mines Affairs, available at 

http://www.bgs.ac.uk/afghanminerals/DMA_tender_docs.htm

British Geological Survey, 2005c, Aynak information package, 

.

in Afghanistan Geological Survey and 

the British Geological Survey, comps., Part IV, The Darband copper deposit: Kabul, Ministry of 

Mines, Department of Mines Affairs, available at 

http://www.bgs.ac.uk/afghanminerals/DMA_tender_docs.htm

Brown, A.C., 1984, Alternative sources of metals for stratiform copper deposits: Precambrian Research, 

v. 25, p. 61–74.

.

Cawthorn, R.G., Barnes, S.J., Ballhaus, Christian, and Malitch, K.N., 2005, Platinum group element, 

chromium, and vanadium deposits in mafic and ultramafic rocks, in

Chernov, V.G., and Fenogenov, A.N., 1980, Osnovnyye cherty stroyeniya svit Loy–Khvar i Aynak v 

Kabul'skoy zone Afganistana [Main structural features of the Loy–Khvar and Ainak suites in the 

Kabul Zone of Afghanistan], Byulleten' Moskovskogo Obshchestva Ispytateley Prirody, Otdel 

Geologicheskiy, v. 55, no. 4, p. 48–56.

Hedenquist, J.W., Thompson, 

J.F., H., Goldfarb, R.J., and Richards, J.P., eds., Economic geology, 100th anniversary volume,

1905–2005: Littleton, Colo., Society of Economic Geologists, p. 215–249.

Chmyrev, V.M., and Azimi, N.A., 1977, The geology and genesis of copper deposits in Kabul region, in

Chmyrev, V.M., Dronov V.I, and others, 1977, Geological structure and commercial minerals of 

Afghanistan: Kabul, Afghanistan Geological Survey Archive. [In Russian.]

V Sc. Conf: Kabul University and Kabul Polytechnical Institute, [unpaginated].

Chmyrev, V.M., Giruvol, T.G., and Teleshev, G.I., 1976, Kabul copper–bearing region, in

Chmyriov, V.M., and others, 1975, Summary on Aynak, Darband, and Jawhar: Russian Geological 

Mission to Afghanistan, [unpaginated].

IV Sc. Conf:

Kabul University and Kabul Polytechnical Institute, [unpaginated].

Cox, D.P., Lindsey, D.A., Singer, D.A., and Diggles, M.F., 2003, Sediment-hosted copper deposits of 

the world—Deposit sub models and database: U.S. Geological Survey Open-File Report 03–107, 

available at http://geopubs.wr.usgs.gov/open-file/of03-107/

Davidson, C.F., 1965, A possible mode of origin of strata-bound copper ores: Economic Geology, v. 60, 

p. 942–954.

.

Davidson, G.J., and Large, R.R., 1998, Proterozoic copper-gold deposits: AGSO Journal of Australian 

Geology and Geophysics, v. 17, no. 4, p. 105–114.

Denikaev, Sh.Sh., Feoktistov, V.P., Pyzhyanov, I.V., Adjruddin, A., Narbaev, Sh.N., and Konev, Yu.M., 

1971, The geology and minerals of the southern part of eastern Afghanistan (an intermediate report by 

the Kabul crew on the work of 1970): Kabul, Department of Geological and Mineral Survey, 

[unpaginated].

Denikaev, Sh.Sh., Pyzhyanov, I.V., Feoktishov, V.P., Adjruddin, A., Narbaev, Sh.N., Konev, Yu.M., 

1971: The Geology and minerals of the southern part of eastern Afghanistan (a preliminary report by 

the Kabul Team on the work in 1970): Kabul, Afghanistan Geological Survey, Archive. [In Russian.]

Doebrich, J.L., and Wahl, R.R., comps., with contributions by Doebrich, J.L., Wahl, R.R., Ludington, 

S.D., Chirico, P.G., Wandrey, C.J., Bohannon, R.G., Orris, G.J., Bliss, J.D., Wasy, Abdul, and 

Younusi, M.O., 2006, Geologic and mineral resource map of Afghanistan: U.S. Geological Survey 

Open File Report 2006–1038, scale 1:850,000, available at

Duke, J.M., 1983, Magmatic segregation deposits of chromite: Geoscience Canada, v. 10, no. 1, 

p. 133–143.

http://pubs.usgs.gov/of/2006/1038/.

Duke, J.M., 1984, Ultramafic-hosted asbestos, in Eckstrand, O.R., ed., Canadian mineral deposit types—

A geological synopsis: Geological Survey of Canada Report 36, p. 67.
Chapter 2A. Summary of the Aynak Copper, Cobalt, and Chromium Area of Interest 91

Duke, J.M., 1996, Podiform (ophiolitic) chromite, in Eckstrand, O.R., Sinclair, W.D., and Thorpe, R.I., 

eds., Geology of Canadian mineral deposit types: Geological Society of America, The Geology of 

North America, v. P–1, p. 621–624. 

Gnos, E., Immenhauser, A., and Peters, T., 1997, Late Cretaceous/Early Tertiary convergence between 

the Indian and African Plates recorded in ophiolites and related sediments: Tectonophysics, v. 253, 

p. 53–64. 

Gusev I.A., Safonov B.A., and others, 1979: Geological structure of the Kabul copper ore field: Kabul, 

Afghanistan Geological Survey Archive. [In English.] 

Gustafson, L. B., and Williams, N., 1981, Sediment-hosted stratiform deposits of copper, lead and zinc, 

in Skinner, B.J., ed., Economic geology, 75th anniversary volume: Littleton, Colo., Society of 

Economic Geologists, p. 139–178. 

Harben, P.W., and Kuzvart, Milos, 1996a, Magnesite and magnesia, in Industrial minerals: A global 

geology: London, Industrial Minerals Information, Ltd., p. 232–246. 

Harben, P.W., and Kuzvart, Milos, 1996b, Talc and soapstone, in Industrial minerals—A global 

geology: London, Industrial Minerals Information, Ltd., p. 407–417. 

Haynes, D.W., 1986a, Stratiform copper deposits hosted by low-energy sediments, in I. Timing of 

sulfide precipitation—An hypothesis: Economic Geology, v. 81, p. 250–265. 

Haynes, D.W., 1986b, Stratiform copper deposits hosted by low-energy sediments, in II. Nature of 

source rocks and composition of metal-transporting water: Economic Geology, v. 81, p. 266–280. 

Hitzman, M., Kirkham, R., Broughton, D., Thorson, J., and Selley, D., 2005, The sediment-hosted 

stratiform copper ore system, in Hedenquist, J.W., Thompson, J.F., H., Goldfarb, R.J., and Richards, 

J.P., eds., Economic geology, 100th anniversary volume, 1905–2005: Littleton, Colo., Society of 

Economic Geologists, p. 609–642. 

Hora, Z.D., 1997, Ultramafic-hosted chrysotile asbestos, in Geological fieldwork 1997: British 

Columbia Ministry of Employment and Investment Paper 1998–1, p. 24K–1–24K–4. 

Jensen, M.L., and Bateman, A.M., 1981, Economic mineral deposits (3d ed., revised): New York, John 

Wiley, 593 p. 

Jowett, E.C., 1986, Genesis of Kupferschiefer Cu-Ag deposits by convective flow of Rotliegende brines 

during Triassic rifting: Economic Geology, v. 8, p. 1723–1837. 

Karim, M., Petrukhin, B.P., Fenogenov, A.N., and Khmelevskoy, V.K., 1992, Elektrometricheskaya 

razvedka mednogo mestorozhdeniya Aynak v Afganistane [Electrometric survey of Aynak copper 

mineralization in Afghanistan]: Izvestiya Vysshikh Uchebnykh Zavedeniy, Geologiya i Razvedka, 

v. 1992, no. 4, p. 158–160. 

Kirkham, R.V., 1989, Distribution, settings, and genesis of sediment-hosted stratiform copper deposits, 

in Boyle, R.W., Brown, A.C., Jefferson, C.W., Jowett, E.C., and Kirkham, R.V. eds., Sediment-hosted 

stratiform copper deposits: Geological Association of Canada Special Paper 36, p. 3–38. 

Kirkham, R.V., Carriere, J.J., Laramee, R.M., and Garson, D.F., 1994, Global distribution of 

sediment-hosted stratiform copper deposits and occurrences: Geological Survey of Canada Open File 

2915b, 256 p. 

Kolotov, B.A., Albul, S.P., Kladovshchikov, V.N., and Ibrakhim R.M., 1981, Rezul'taty 

gidrogeokhimicheskogo metoda poiskov v Kabul'skom mednorudnom rayone Afganistana 

[Hydrochemical prospection results in Kabul copper ore region, Afghanistan]: Izvestiya Vysshikh 

Uchebnykh Zavedeniy, Geologiya i Razvedka, v. 1981, no. 6, p. 80–89. 

Koons, P.O., 1981, A study of natural and experimental metasomatic assemblages in an ultramaficquartzofeldspathic metasomatic system from the Haast Schist, South Island, New Zealand: 

Contributions to Mineralogy and Petrology, v. 78, p. 189–195. 

Kramer, D.A., 2001, Magnesium, its alloys and compounds: U.S. Geological Survey Open-File Report 

01–341, available at http://pubs.usgs.gov/of/2001/of01-341/. 
92 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

Kubatkin, L.V., Voinov, V.N., Kracov, N.V., Murtazin, A.M., 1978: Results of the geophysical survey 

in the Kabul copper ore field (results for years 1974–77) : Kabul, Afghanistan Geological Survey, 

Archive. [In Russian.] 

Kutkin, I.S. and Gusev, I.A. 1977: Geological setting of the Dzhavkhar group occurrences and their 

evaluation, Kabul copper-ore region: Kabul, Afghanistan Geological Survey, Archive. [In Russian.] 

Laznika, P., 1981, Data on the worldwide distribution of stratiform and stratabound ore deposits, chap. 2 

of Wolf, K.H., ed., Handbook of stratiform and stratabound ore deposits, Part III: Elsevier Science 

Ltd., p. 79–389. 

Lindsey, D.A., 1982, Copper shales, in Erickson, R.L., ed., Characteristics of mineral deposit 

occurrences: U.S. Geological Survey Open-File Report 82–795, p. 196–199. 

Ludington, Steve, Orris, G.J., Bolm, K.S., Peters, S.G., and the U.S. Geological Survey-Afghanistan 

Ministry of Mines and Industry Joint Mineral Resource Assessment Team, 2007, Preliminary mineral 

resource assessment of selected mineral deposit types in Afghanistan: U.S. Geological Survey 

Open-File Report 2007–1005, 44 p., available at http://pubs.usgs.gov/of/2007/1005/. 

MacKevett, E.M., Jr., Cox, D.P., Potter R.W., II, and Silberman, M.L., 1997, Kennecott-type deposits, 

Wrangell Mountains, Alaska: High-grade copper deposition near a limestone-basalt contact, in

Goldfarb, R.J., and Miller, L.D., eds., Mineral deposits of Alaska: Economic Geology Monograph 9, 

p. 66–89. 

McCarthy, E.F., Genco, N.A., and Reade, E.H., Jr., 2006, Talc, in Kogel, J.E., Trivedi, N.C., Barker, 

J.M., and Krukowski, S.T., eds., Industrial minerals and rocks (7th ed.): Littleton, Colo., Society for 

Mining, Metallurgy, and Exploration, Inc., p. 971–986. 

Minchenok, J.M., Sergejev, V.V., Krasnov, V.P., Koloskov, V.P., 1979, The report of the results of 

prospecting and evaluation survey at the Darband copper deposit in the years 1974–1979: Kabul, 

Afghanistan Geological Survey, Archive. [In Russian.] 

Nevretdinov, E.B., and Mirzamon, M., 1979, Report on prospecting—Survey and evaluation works on 

asbestos, chromite and other raw material in the northern part of the Logar Ultramafic Massif in 1978: 

Kabul, Afghanistan Geological Survey, Archive. 

Obolenskiy, A.A., Rodionov, S.M., Ariunbileg, Sodov, Dejidmaa, Gunchin, Distanov, E.G., Dorjgotov, 

Dangindorjiin, Gerel, Ochir, Hwang, Duk Hwan, Sun, Fengyue, Gotovsuren, Ayurzana, Letunov, 

S.N., Li, Xujun, Nokleberg, W.J., Ogasawara, Masatsugu, Seminsky, Z.V., Smelov, A.P., Sotnikov, 

V.I., Spiridonov, A.A., Zorina, L.V., and Yan, Hongquan, 2003, Mineral deposit models for northeast 

Asia, in Nokleberg, W.J., and others, eds., Preliminary publications book 2 from project on mineral 

resources, metallogenesis, and tectonics of northeast Asia: U.S. Geological Survey Open–File Report 

03–203 (CD–ROM), 47 p. 

Orris, G.J., 1986, Grade and tonnage model of serpentine-hosted asbestos, in Cox, D.P., and Singer, 

D.A., Mineral deposit models: U.S. Geological Survey Bulletin 1693, p.46–48. 

Page, N.J, 1986, Descriptive model of serpentine-hosted asbestos, in Cox, D.P., and Singer, D.A., 

Mineral deposit models: U.S. Geological Survey Bulletin 1693, p.46. 

Page, N.J, 1998a, Preliminary descriptive model of ultramafic-hosted talc, in Orris, G.J., ed., Additional 

descriptive models of industrial mineral deposits: U.S. Geological Survey Open-File Report 98–505, 

p. 5–7. 

Page, N.J, 1998b, Preliminary descriptive model of ultramafic-hosted magnesite, in Orris, G.J., ed., 

Additional descriptive models of industrial mineral deposits: U.S. Geological Survey Open-File 

Report 98–505, p. 2–4. 

Paradis, S., and Simandl, G.J., 1996, Cryptocrystalline ultramafic-hosted magnesite veins, Lefebure, 

D.V., and Hoy, T, eds., Selected British Columbia mineral deposit profiles, v. 2—Metallic deposits: 

British Columbia Ministry of Employment and Investment Open-File Report 1996–13, p. 97–100. 
Chapter 2A. Summary of the Aynak Copper, Cobalt, and Chromium Area of Interest 93

Peters, S.G., Ludington, S.D., Orris, G.J., Sutphin, D.M., Bliss, J.D., and Rytuba, J.J., eds., and the 

U.S. Geological Survey-Afghanistan Ministry of Mines Joint Mineral Resource Assessment Team, 

2007, Preliminary non-fuel mineral resource assessment of Afghanistan: U.S. Geological Survey 

Open-File Report 2007–1214, 810 p., 1 CD–ROM. (Also available at 

http://pubs.usgs.gov/of/2007/1214/

Plotnikov, G.I. and Slozhenikin, A.P., 1968, Report on the results and revised evaluation work of 

copper, lead–zinc, and gold occurrences in Afghanistan carried out in 1967: Kabul, Department of 

Geological and Mineral Survey, [unpaginated].

.)

Pohl, W., 1990, Genesis of magnesite deposits—Models and trends: Geologische Rundschau, v. 79, 

no. 2, p. 291–299.

Rose, A.W., 1976. The effect of cuprous chloride complexes in the origin of red-bed copper and related 

deposits, Economic Geology, v.71, p. 1036–1048.

Rose, A.W., and Bianchi-Mosquera, G.C., 1993, Adsorption of Cu, Pb, Zn, Co, Ni, and Ag on goethite 

and hematite—A control on metal mobilization from red beds into stratiform copper deposits: 

Economic Geology, v. 88, p. 1226–1236.

Ruan Huichu, Hua Renmin, and Cox, D.P., 1991, Copper deposition in deformed strata adjacent to a salt 

diapir, Dongchuan Area, Yunnan Province, China: Economic Geology v. 86, p. 1539–1545.

Ruffell, A.H., Moles, N.R., and Parnell, J., 1997, Characterization and prediction of sediment-hosted ore 

deposits using sequence stratigraphy: Ore Geology Reviews, v. 12, p. 207–223.

Shcherbina, Yu.I., Petrov, S.E., and Silkin, V.G., 1975, The geology and minerals of the central part of 

the Kabul median mass: Kabul, Department of Geological and Mineral Survey, [unpaginated].

Shride, A.F., 1973, Asbestos, in

Sidiki, Atikulla, 1978, O novom stratiformnom mestorozhdenii medi v Afganistane, [A new stratified 

copper deposit in Afghanistan]: Zapiski Leningradskogo, Ordena Lenina, Ordena Oktyabr'skoy 

Revolyutsii i Ordena Trudovogo Krasnogo Znameni Gornogo instituta im G.V. Plekhanova, v. 75, 

p. 28–30.

Brobst, D.A., and Pratt, W.P., eds., United States mineral resources: 

U.S. Geological Survey Professional Paper 820, p. 63–73.

Siebdrat, H.G., 1965, Parallelisierung von optisch ermittelter und analytisch berechneter 

mineralzusammensetung bei chromiterzen Afghanistans: Bergbauwissenschaften Jb., v. 12H 1⁄2, 

p. 28–34. [In German.]

Siebdrat, H.G., 1971, Chromite in ultrabasischen magmatiten des unteren Logar-Tales SudostAfghanistan: Beih. Geol. Jb., v. 96, p. 209–226. [In German.]

Simandl, G.J. and Ogden, D.,1999, Ultramafic-hosted talc-magnesite, in Simandl, G.J., Hora, Z.D., and 

Lefebure, D.V., eds., Selected British Columbia mineral deposit profiles, v. 3, Industrial minerals: 

British Columbia Ministry of Energy and Mines, available at http://www.em.gov.bc.ca/Mining/

GeolSurv/MetallicMinerals/MineralDepositProfiles/profiles/m07.htm.

Singer, D.A., and Page, N. J, 1986, Grade and tonnage model of minor podiform chromite, in Cox, D.P., 

and Singer, D.A., eds., Mineral deposit models: U.S. Geological Survey Bulletin 1693, 379 p., 

available at http://pubs.usgs.gov/bul/b1693/html/bullfrms.htm.

Singer, D.A., Page, N. J, and Lipin, B.R., 1986, Grade and tonnage model of major podiform chromite, 

in Cox, D.P., and Singer, D.A., eds., Mineral deposit models: U.S. Geological Survey Bulletin 1693, 

379 p., available at http://pubs.usgs.gov/bul/b1693/html/bullfrms.htm.

Slavin, V.I., Fedorov T.O., and Feruz N.M., 1972: The geology and age of the metamorphic complex in 

the Kabul district: “Vestnik MSU”, Moscow.

Selley, David, Broughton, David, Scott, Robert, Hitzman, Murray, Bull, S.W., Large, R.R., McGoldrick, 

P.J., Croaker, Mawson, Pollington, Nicky, and Barra, Fernando, 2005, A new look at the geology of 

the Zambian copperbelt, in Hedenquist, J.W., Thompson, J.F., Goldfarb, R.J., and Richards, J.P., eds., 

Economic Geology, 100th anniversary volume, 1905–2005: Littleton, Colo., Society of Economic 

Geologists, Littleton, p. 965–1000.
94 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

Sverjensky, D.A., 1987, The role of migrating oil field brines in the formation of sediment-hosted 

Cu-rich deposits: Economic Geology, v. 82, p. 1130–1141. 

Sverjensky, D.A., 1989, Chemical evolution of basinal brines that formed sediment-hosted Cu-Pb-Zn 

deposits, in Boyle, R.W., Brown, A.C., Jefferson, C.W., Jowett, E.C., and Kirkham, R.V., eds., 

Sediment-hosted stratiform copper deposits: Geological Association of Canada Special Paper 36, 

p. 127–134. 

Sweeney, M.A. and Binda, P.L., 1989, The role of diagenesis in the formation of the Konkola Cu-Co 

orebody of the Zambian copperbelt, in Boyle, R.W., Brown, A.C., Jefferson, C.W., Jowett, E.C., and 

Kirkham, R.V., eds., Sediment-hosted stratiform copper deposits: Geological Association of Canada 

Special Paper 36, p. 499–518. 

Tapponnier, Paul, Mattauer, Maurice, Proust, Francois, and Cassaigneau, Christian, 1981, Mesozoic 

ophiolites, sutures, and large-scale tectonic movements in Afghanistan: Earth and Planetary Science 

Letters, v. 52, p. 355–371. 

United Nations Economic and Social Commission for Asia and the Pacific, 1995, Atlas of mineral 

resources of the ESCAP region—Geology and mineral resources of Afghanistan: United Nations 

Economic and Social Commission for Asia and the Pacific, 150 p. [Available from the National 

Technical Information Service, Springfield, Va., as NTIS Report UN–0561.] 

U.S. Geological Survey, 2000, U.S. talc—Baby powder and much more: U.S. Geological Survey Fact 

Sheet 065–00, 1 sheet, 2 p. 

Virta, R.L., 2002, Asbestos—Geology, mineralogy, mining, and uses: U.S. Geological Survey 

Open-File Report 02–149, available at http://pubs.usgs.gov/of/2002/of02–149/. 

Virta, R.L., 2007, Asbestos, in Metals and minerals: U.S. Geological Survey Minerals Yearbook 2005, 

v. 1, p. 8.1–8.6. 

Volin, M.E., 1950, Chromite deposits in Logar Valley, Kabul Province, Afghanistan: Washington, D.C., 

U.S. Bureau of Mines Report, 58 p. 

Wrucke, C.T., 1995, Serpentine-and carbonate-hosted asbestos deposits, in du Bray, E.A., ed., 

Preliminary compilation of descriptive geoenvironmental mineral deposit models: U.S. Geological 

Survey Open–File Report 95–831, p. 39–46, available at http://greenwood.cr.usgs.gov/pub/open-filereports /ofr-95-0831/.

Yashchinin, S.B., Bakarasov, Ye.V., Mogilin, V.S., Grischenko, V.I., Danchev, V.V., Malkov, I.I., 

Makhmutov, T.T., Moyseev, V.S., Cheremicyn, V.G., Shcherbonos, V.D., Yurgenson G.A., 1978: 

The report on the detailed survey of the central prospect of the Aynak copper deposit with reserves 

calculation up to April: Kabul, Afghanistan Geological Survey, v. 1 to 9, v. 10 (parts 1 to 4). [In 

Russian.] 

Yashchinin, S, B., and Giruval', T., 1981, Aynakskoye mestorozhdeniye medi [The Ainak copper 

deposit, Afghanistan]: Sovetskaya Geologiya [Soviet Geology], v. 1981, no. 7, p. 78–82. 

Yurgenson, G.A., Akram, A.M., Dzhelani, K.G, and Gavrilov, A.M., 1981, Mineralnyye tipy rud i 

posledovatel'nost' obrazovaniya sul'fidov na mestorozhdenii medi Aynak (Respublika Afganistan), 

[Type minerals of ores and sulfide sequence in Ajnak copper deposit, Afghanistan]: Izvestiya 

Vysshikh Uchebnykh Zavedeniy, Geologiya i Razvedka, v. 1981, no. 6, p. 150–153. 

Yurgenson, G.A., Gavrilov, A.M., and Il'menev, Ye.S., 1985, Mineraly kobal'ta mestorozhdeniya medi 

Aynak [Cobalt minerals of the Aynak copper deposit]: Zapiski Vsesoyuznogo Mineralogicheskogo 

Obshchestva, v. 114, no. 4, p. 428–434. 

Zaycev, V.N., Bereziy, A.Ye., Bushmelev, Ye.N., Kerimov, A.F., Maydancev, G.A., Miroshnikov, 

K.Ye., Sadik, M.A., Tkachev, M.M., Troickiy, S.V., Chzhen, V.V., Sholin, V.G., 1988: The report on 

the results of the preliminary survey of the western prospect of the Aynak copper deposit with reserves 

calculation up to July 1: Kabul, Afghanistan Geological Survey, 10 v.