Chapter 7A. Summary of the Haji-Gak Iron Area of Interest

Contribution by Karine Renaud, David M. Sutphin, Stephen G. Peters, and Lawrence J. Drew

Abstract

The Haji-Gak iron area of interest in Bamyan, Parwan, and Wardak Provinces contains the 

Haji-Gak iron deposit and several other prospects and deposits. Three subareas have been delineated 

within the main area of interest. The Haji-Gak iron deposit (prospect subarea) in Bamyan Province is the 

best known and largest iron oxide deposit in Afghanistan. The Haji-Gak ore deposit is more than 

12 kilometers (km) long and 3 kilometers (km) wide and contains 16 separate zones, some of which are 

as much as 5 km in length, 380 meters (m) wide and extend 550 m downdip. Seven of these zones have 

been studied in detail. Iron ore is primary and oxide. The primary ore [80 volume percent (vol. %) of the 

deposit] is present below 130 m, comprises mostly magnetite and pyrite as well as smaller amounts of 

other sulfide minerals, including chalcopyrite, and averages 61.3 weight percent (wt. %) iron. The 

remaining 20 vol. % of the iron ore is oxidized and consists of three hematitic ore types at slightly 

higher grades (more than 62.0 wt. %). The mineralization is structurally controlled. A previous Russian 

resource estimate for the entire deposit is 1,700 million metric tons (Mt), although the mining reserve 

estimate for the near surface oxide ore in the most explored area is 85 Mt.

The Chuy, Khaish, Khakriz, Kharzar, and Zerak sedimentary-rock-hosted iron deposits are 

adjacent and to the east of the main Haji-Gak iron deposit in the Northeastern Haji-Gak subarea and 

have also been explored. The Haji-Gak iron area of interest also contains barite deposits and 

mineralization near the Haji-Gak prospect subarea and in the Northeastern and Farenjal subareas. The 

Haji-Gak barite deposit in the Haji-Gak prospect subarea fills veins over an area of 10 square kilometers 

(km2

). The speculative resources of the largest vein are 36,200 metric tons with an average barium oxide 

content of 56 wt. % barium oxide. Additionally, the Haji-Gak prospect subarea contains the Haji-Gak 

limestone deposit with speculative resources over an area of 45 km2 to a depth of 60 m and reported 

resource of 3.5 Mt. The Haji-Gak sandstone, also in the Haji-Gak prospect subarea, grades from 93.66 to 

97.31 wt. % silicon oxide and contains speculative resource of 650,000 metric tons. Speculative 

resources are undiscovered resources that occur in unknown and undiscovered types of deposits in 

favorable geologic settings or in unknown types of deposits that have to be recognized. The quality of 

the silicon oxide raw material is suitable for manufacturing class-II dinas. 

In the northeastern part of the Haji-Gak iron area of interest, Paleozoic strata contain the Farenjal 

barite and lead-zinc ore district. The subordinate mineralization consists of asbestos, copper, iron, 

manganese, and talc.

Extensive exploration has been done in the Haji-Gak prospect subarea for iron deposits. Afghan, 

French, German, and Russian feasibility studies on the main iron deposit were completed. The 

remainder of the Haji-Gak iron area of interest has not been explored to this level. A U.S. Geological 

Survey team visited the lower parts of the ore deposit area briefly in 2006 and 2009. 

7A.1 Introduction

This chapter is a summary and interpretation of Kusov and others (1965b), correlating the report 

with the results of joint geologic and compilation activities conducted during 2009 to 2011 by the 

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

Operations (TFBSO), and the Afghanistan Geological Survey (AGS) (fig. 7A–1; table 7A–1) in the 

Haji-Gak iron area of interest (AOI) and subareas. Accompanying complementary chapters 7B, 7C, and 

7D additionally address hyperspectral data, geohydrologic, and ore reserve assessments respectively of 
Chapter 7A. Summary of the Haji-Gak Iron Area of Interest 451

the Haji-Gak iron AOI. Supporting AOI data and information for this chapter are available from the 

Ministry of Mines in Kabul.

We have attempted to translate the original Russian terminology and rock classification into 

modern English geologic usage as literally as possible without changing any implied genetic or process 

oriented implications in the original descriptions, using the age presented in the original report. A more 

recent study of the Haji-Gak area (Kusov, 1965a) substantially modified the ages for the Haji-Gak 

Formation from Proterozoic to Devonian and provided new interpretations of the geologic settings in 

which various units were deposited. 

The Haji-Gak iron AOI is in east-central Afghanistan and consists of a main area and three 

subareas. The main area is 2,079 square kilometers (km2) the Farenjal subarea is 557 km2, the Northeast 

(NE) Haji-Gak subarea is 381 km2, and the Haji-Gak prospect subarea is 180 km2 (fig. 7A–2). The 

Haji-Gak iron AOI is located in parts of the Bamyan, Parwan, and Wardak Provinces and parts of the 

Bamyan, Beshud, Ghorband, Hisa-i-Awal, Markazi, Shekh Ali, Shibar, and Surkh-i-Parso Districts. 

Deposit types that are expected or known in the Haji-Gak iron AOI are Algoma iron, bedded barite, 

sandstone, and limestone. 

7A.2 Previous Work

The Haji-Gak iron deposit has been explored since 1911, and geologic and engineering work has 

been summarized in many Soviet reports; however, modern reconnaissance and prospecting work did 

not start until 1965. The first recorded geologic exploration was by G. Hyden, Director of the Geological 

Survey of India, who explored the Haji-Gak iron deposit for the first time in 1911. During this 

expedition, a stratigraphic sequence for the area was constructed, and three formations were identified, 

along with their ages; the formations were Kalu (Awband Formation) of Early Devonian age, Haji-Gak 

of Devonian age, and Helmand of Carbonaceous age. 

The Haji-Gak iron deposit was further investigated by K. Brueckl (1935, 1936), Popol and 

Tromb (1954), Bybochkin and Kurotchenko (1960), Momji and Chaikin (1960), de Lapparent (1961), 

and Mirzad (1961). 

In Brueckl (1935, 1936) the hydrothermal siderite veins in the deposit and the hornblende 

granitic intrusion that was cut by these siderite veins were described and categorized. Brueckl (1935, 

1936) proposed that formation of magmatic hydrothermal siderite veins, and by inference the iron ores, 

were genetically and spatially related to the granite. The hypotheses on iron ore genesis were bolstered 

by Bybochkin and Kurotchenko (1960) and Momji and Chaikin (1960). 

Table 7A–1.

[Tabulation of data from Soviet exploration in the 1960s. NA, not available]

Reserves and resources of the Haji-Gak iron deposit. 

Soviet

category Equivalent classification Ore type

Reserve, 

million metric 

tons of ore

Iron, weight 

percent

Sulfur, weight 

percent

A Measured or proven Oxidized ore 9.1 62.52 0.14

B Measured or proven Oxidized ore 19.2 62.69 0.09

C1 Indicated or probable Oxidized ore 65.1 62.15 0.13

C1 Indicated or probable Primary ore 16.2 61.3 4.56

C1 Indicated or probable Fragmental ore 1.2 60.62 0.08

C2 Inferred or possible All ore types 3,143 NA NA

C2 Inferred or possible Fragmental ore 2.9 NA NA

P2 Hypothetical resources All ore types 1,333.3 NA NA

P2 Hypothetical resources Fragmental ore 8.6 NA NA

Total 1,769.9
452 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

Figure 7A–1. LANDSAT image of the Haji-Gak iron area of interest (outlined in red), showing subareas (color-shaded areas) and major prospects 

(brown and blue triangles) and mineral occurrences (red and yellow circles). Data are from Peters and others (2007, p. 118–122).
Chapter 7A. Summary of the Haji-Gak Iron Area of Interest 453

Figure 7A–2.

Popol and Tromb (1954) identified schist and three sedimentary sequences (from top to bottom), 

as follows: schist and limestone, red layers, and coarse-grained conglomerate. Devonian fauna was 

found in limestone. These sequences overlay the Kalu Formation that is in turn overlain by the Helmand 

Formation. 

Map showing the location of the Haji-Gak area of interest and subareas.

In de Lapparent, (1961) the Haji-Gak iron deposit was identified as an exhalative deposit, which 

suggested the deposit had undergone two types of metamorphism—greenschist facies and sericite 

dynamic-metamorphism.

The most extensive information about the deposit and its resources was provided by Momji and 

Chaikin (1961), Bybochkin and Kurotchenko (1961), and Mirzad (1961). 

Most of the detailed prospecting has been done on the western part of Haji-Gak iron mineralized 

zone. This work was carried out by Russian and Afghan geologists and has been documented in many 

reports listed in the Selected References section of this chapter. This exploration is well documented by 

Kusov and others (1965a,b) and includes prospect and geological maps at different scales (fig. 7A–3). 

The work included the drilling of 4 holes, opening of 15 adits and 29 trenches, and hand specimen and 

microscopic description of ores and minerals, calculation of ore reserves, and the study of hydrogeology 

of the region. 

Exploration and geologic work terminated in 1989 with the withdrawal of the Soviet army and 

the civil war that interrupted further activity by the Afghanistan Geological Survey (AGS). Although the 

AGS was able to preserve many of the Soviet reports, some of the reports were destroyed. The condition 

of the reports and maps ranges from poor to excellent., 

7A.3 Metallogeny

Iron deposits hosted in sedimentary rocks in Afghanistan mainly are present within Proterozoic 

sedimentary and volcanic-sedimentary rock packages (Peters and others, 2007, p. 118–122). Most iron 

deposits, including the large Haji-Gak iron ore deposit and its associated deposits, are present along a 

tectonized zone in the Har-i-Rod Fault zone in central Afghanistan. Additionally, an oolitic ironstone 

mineral occurrence also is known in the Late Paleozoic to Cenozoic sedimentary rocks (Nishiwak, 

1970). Hematite vein deposits also are present in Proterozoic, Permian, and Oligocene rocks. Other 

major iron deposits in Afghanistan are in iron skarn bodies mainly around Oligocene intrusive bodies in 

the Kandahar and Badakshan Provinces. Some geologists believe that the Proterozoic-hosted deposits 

are products of contact metamorphism around the Oligocene intrusive bodies (Peters and others, 2007, 

p. 118–122).
454 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

Figure 7A–3. Examples of illustrations from Soviet-era reports (Kusov and others, 1965a,b) on the Haji-Gak iron 

deposit. (a) Geologic prospecting plan of the western area of Haji-Gak; (b) Cross-sections used for calculations of 

ore reserves; and (c

The main ore minerals within the sedimentary iron deposits in Afghanistan are hematite and 

magnetite and hematite, with smaller amounts of martite. The metallogenic age, mineralogy, textures, 

and sizes of the deposits make them compatible with several model types, such as Superior iron 

) Drill hole logs used for calculation of ore reserves. This scan is presented as an example of 

the style and type of study and reporting work that has been done in the past.
Chapter 7A. Summary of the Haji-Gak Iron Area of Interest 455

deposits, Algoma iron deposits, and iron oxide copper-gold deposits. Sedimentary manganese deposits 

are a deposit type commonly associated with many sedimentary iron deposits throughout the world. 

A permissive area for the occurrence of Haji-Gak-type iron deposits in Afghanistan was 

delineated by Peters and others (2007, p. 118–122) to encompass all Neoproterozoic sedimentary host 

rocks, which consist of greenschist facies schistose and phyllitic marble, dolomite, sandstone, and 

metavolcanic rocks (map unit Z1scp) as well as associated Neoproterozoic metavolcanic andesite lava 

and interlayered sedimentary rocks (map unit Z1

A southern part of the permissive area lies to the southwest of the Haji-Gak iron AOI and 

contains the Mangasak iron occurrence in Wardak Province and an unnamed stratabound manganese 

occurrence in northeastern Uruzgan province (fig. 7A–7). The Mangasak occurrence lies along the 

contact between Proterozoic gneiss and schist layers in a 1,200-meter (m)-long and 50- to -100-m-wide 

altered carbonated zone that contains magnetite as disseminations, nodules, and veinlets (Karapetov and 

others, 1970). The unnamed manganese occurrence consists of 1.5-m by 7-m lenses within 

Neoproterozoic cherty marl rocks (Abdullah and others, 1977). 

al) (fig. 7A–4). Parts of the permissive tract outside the 

Haji-Gak iron area of interest are located in northern Kandahar, Zabul, Uruzgan, Ghazni, and Parwan 

Provinces (fig. 7A–4). A number of more favorable areas were also delineated to encompass the geology 

hosting deposits or occurrences like Haji-Gak (figs. 7A–5 and 7A–6). The updated favorable tract 

contains the Haji-Gak, Kharzar, Khaish, Chuy, Kharkiz, Darre-i-Neelee, and Zerak sedimentary-rockhosted iron deposits (fig. 7A–6).

Lack of unique and detailed descriptions of the Haji-Gak iron deposit at the time of assessment 

and questions concerning its genesis did not allow adequate model selection and this hampered the 

ability of the USGS Assessment Team in 2007 to make a quantitative assessment of the permissive area 

(Peters and others, 2007, p. 118–122). The main deposit types considered during the assessment process 

were Lake Superior-type iron deposits (Cannon, 1986a), Algoma iron deposits (Cannon, 1986b) and iron 

oxide copper-gold deposits (Cox, 1986; Haynes, 2000; Hitzman, 2000). After further study, the model 

that most closely resembles the Haji-Gak iron deposits is the Algoma iron type deposit, which is hosted 

by volcanogenic iron-bearing sequences mostly of Archean or Proterozoic age, similar to the Awband 

Formation at Haji-Gak. The Algoma iron type deposits form microbanded to mesobanded lenticular 

shapes that are less than 50 m thick and occasionally extend for more than 10 kilometers (km) along 

strike (Bekker, 2010), similar to the Haji-Gak iron deposit. Rock types that are associated with Algoma 

iron type deposits usually are mafic to felsic submarine volcanic rocks and deep-water clastic and 

volcanoclastic sediments. The textures of rocks in these iron deposits are pillowed greenstone, 

intermediate to felsic tuff and agglomerate, and poorly sorted clastic sediments (Cannon, 1986a,b). 

Individual volcanic rock layers are interbedded with deepwater greywacke and mudrocks. 

7A.4 Known Deposits

The Haji-Gak iron AOI contains the Haji-Gak iron deposit (prospect subarea) in Bamyan 

Province and a number of other sedimentary rock-hosted deposits. Additionally there are several other 

deposits and prospects in the AOI and its subareas. The Haji-Gak iron deposit is the best known iron 

oxide deposit in Afghanistan, and similar occurrences of this type have been identified along a 600-kmlong discontinuous east-west belt. The deposit is more than 12 km long and 3 km wide and contains 16 

separate zones, some of which are up to 5 km long, 380 m wide, and extend 550 m downdip; seven of 

these zones have been studied in detail. 
456 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

Figure 7A–4. Map of the Haji-Gak Neoproterozoic permissive tract sedFe-01 and the Paleoproterozoic 

permissive tract sedfe02 that contains undiscovered sedimentary-rock-hosted iron deposits, showing distribution of 

Proterozoic rocks that host the Haji-Gak iron deposit from Peters and others (2007). The red star is Kabul.
Chapter 7A. Summary of the Haji-Gak Iron Area of Interest 457

Figure 7A–5. Map showing parts of the permissive sedFe-01 Haji-Gak tract that contains the Haji-Gak and related 

deposits from Peters and others (2007).
458 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

Figure 7A–6. Maps showing the location of the favorable sedFe-01-f1 Haji-Gak tract within larger permissive tract sedFe-01 tract from Peters and others 

(2007). (a) General location of favorable tract sedFe-01-f1. (b) Geologic units within and surrounding the Haji-Gak deposit. Host units within the tract consist 

of Z1scp, Neoproterozoic greenschist, marble, dolomite, metavolcanic rocks including phyllite, schist, and sandstone; Z1al, Neoproterozoic marble, dolomite, 

and metavolcanic rocks; DCld, Late Devonian to Mississippian limestone, dolomite, and schist;; and CP1ssl , Carboniferous to Early Permian sandstone, 

siltstone, shale, and mafic volcanic rocks.
Chapter 7A. Summary of the Haji-Gak Iron Area of Interest 459

Figure 7A–7. Map showing southern parts of the permissivesedFe-01 Haji-Gak tract for undiscovered 

sedimentary iron deposits from Peters and others (2007). The southern parts of the tract contain the Mangasak iron 

occurrence and a stratabound unnamed manganese deposit to the southwest.
460 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

Figure 7A–8. Photograph of a banded hydrogoethite-hematite-semimartite. The light bands are made of 

hematite, and the black bands are made of magnetite, martite, and hydroxides. The sample in the photograph is 

from drill hole # 2 at a depth of 36.30 meters (Kusov and others, 1965a,b).

Iron ore is both primary and semioxide. The primary ore [80 volume percent (vol. %) of the 

deposit] is present below 130 m and comprises magnetite, pyrite, and minor other sulfide minerals, 

including chalcopyrite, and averages 61.3 weight percent (wt. %) iron. The remaining 20 vol. % of the 

ore is oxidized and consists of three hematitic ore types at slightly higher grades than the primary ore. 

The mineralization is structurally controlled. Previous Russian resource estimates for the entire deposit 

are 1,700 million metric tons (Mt), although the mining reserve estimate for the near-surface oxide ore 

in the most explored area is 85 Mt (table 7A–1; Momji and Chaikin, 1960; Mirzad, 1961; Kusov, 1963; 

Kusov and others, 1965a,b; Bouladon and de Lapparent1975; Abdullah and others, 1977). 

The Haji-Gak orebody no. 1 extends 5 km, the strike of the deposit is southeasterly at 140° to 

150o with a dip angle of 60° to 70o, and is 110 m thick. The Haji-Gak iron orebodies cover an area of 

35 km2. There are six drill holes, two adits and three reserves of about 20 Mt of ore (table 7A–1). The 

deposit was discovered in 1911 by G.T. Hyden of the Indian Geological Survey. The mineral 

composition of the Haji-Gak orebody no. 1 is 30 vol. % magnetite, 25 vol. % hydroxides, 20 vol. % 

martite, 7 vol. % quartz, and 5 vol. % hematite (Sutphin and others, 2010). 
Chapter 7A. Summary of the Haji-Gak Iron Area of Interest 461

Figure 7A–9. Diagram of the environment most likely for the formation of sedimentary and volcanogenic iron deposits. The diagram shows the formation of 

Algoma iron type deposits near the Volcanic arc and Lake Superior type deposits near the upper shelf. Rocks of each type of deposit are represented. The 

Haji-Gak iron deposit contains rocks more closely related to volcanoclastic settings. Diagram modified from Gross (1973) and Peters (2010).
462 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

7A.5 Geology of the Haji-Gak Iron Deposit Area

The 1:1,000,000-scale geologic map of Doebrich and Wahl (2006) shows the Haji-Gak iron 

deposit to be hosted in Neoproterozoic sedimentary rocks, which are described as greenschist facies 

schistose and phyllitic marble, dolomite, sandstone, and metavolcanic rocks (map unit Z1scp). The 

deposit is also interbedded with Neoproterozoic metavolcanic andesite lava and interlayered 

sedimentary rocks (map unit Z1

The oldest part of the Haji-Gak Proterozoic stratigraphic succession, as described by Kusov and 

others (1965a,b), is the Neoproterozoic Kab Formation that contains quartz-sericite schist, phyllite, 

marble, and dolomite and porphyrite lenses (fig.7A–11). The Haji-Gak iron deposit is hosted by the 

Neoproterozoic Awband Formation, which, together with the underlying Kab Formation, forms the 

4,500-m-thick Qala Group, a sequence of metavolcanic and metasedimentary rocks that comprise tuff, 

argillaceous rocks, and minor chert and marble

al).

.

Intrusive complexes are present in the Proterozoic rocks of Haji-Gak iron deposit area. The 

oldest consists of small intrusions of quartz porphyry, plagiogranite, and quartz diorite, including 

granodiorite. The youngest includes sills, dikes, and small stocks of diabase. In addition, there are local 

occurrences of keratophyre and metasomatic carbonatite. Serpentine bodies also are present and 

comprise thin (up to 5-m) sills and dikes with microflaky and spotted textures. The serpentine rocks are 

green, schistose, and fine-grained. The primary mineralogy of the serpentine rock has been converted to 

secondary antigorite, talc, and magnesite as well as later minerals, such as brucite and carbonate, that are 

mostly developed in the Jowqul Formation and more rarely in the Kharzar Formation. 

 The Awband Formation comprises sericite and quartzsericite schist, sandy quartz sericite schist, carbonate chlorite-sericite schist, marble, dolostone, and 

plagioporphyrite with scapolite, volcanic rocks, and tuff. The iron orebodies in the Neoproterozoic 

Awband Formation are overlain by the Green Schist Formation (fig. 7A–11) that is dominated by 

quartz-chlorite-sericite schist and quartz-chlorite schist, plagioporphyrite with scarce scapolite, and 

metavolcanic rocks that locally are intruded by granodiorite (figs. 7A–12, 7A–13, and 7A–14).

These Paleoproterozoic volcanoclastic rocks are unconformably overlain by the Upper Devonian 

Haji-Gak Formation that contains remnants of corals and brachiopods and comprises grey-black 

limestone injected with a thick network of white, coarse-crystalline barite veins, calcareous 

conglomerate and breccias, calcareous-clayey shale, sandy limestones, calcareous sandstones, and 

quartzite (figs. 7A–11 and 7A–15). The Lower Carboniferous Kharzar Formation unconformably 

overlies the Haji-Gak Formation and contains shale, sandstone, and quartzite. These formations are as 

thick as 500 to 900 m.

The Quaternary rocks are Holocene to Recent floodplain and fluvial, alluvial-colluvial, and 

fluvioglacial moraine deposits and glacial outwash. The deposits of fragmental iron ore are located in 

Recent colluvial deposits (figs. 7A–11 and 7A–15).

The Haji-Gak iron orebody and its host rocks are folded and faulted (fig. 7A–15). The 

predominant strike of the Proterozoic and Paleozoic rocks is between northeast and north-northeast, with 

a regional dip of approximately 50° towards the south-southeast or southeast and a general plunge of 

mesoscopic and macroscopic folding to the southeast (fig. 7A–16a,b). Strikes and dips of bedding and 

bedding plane parallel foliation were compiled in the study in 11 separate structural domains in the main 

Haji-Gak iron deposit area from the maps of Kusov and others (1965a,b) and these data were plotted as 

poles to planes and then contoured on equal area stereonets (fig. 7A–16a). Strikes of the fold axial 

planes were identified from inferred folding of the ore on the map, and dips of the axial planes were 

approximated from the stereonet plots. The results of this analysis confirmed that the dominant plunge 

of folds in the host rocks and the contained ores is about 40° to 50° southeast (fig. 7A–16a

One major steeply dipping fault has juxtaposed the Neoproterozoic rocks against the crystalline 

Mesoproterozoic rocks (fig. 7A–15). Another fault has thrown Upper Devonian rocks against the 

Neoproterozoic Green Schist Formation. In addition, a number of north-south and north-west trending 

faults, some of which are probably thrusts, offset parts of the Neoproterozoic succession, including the 

).
Chapter 7A. Summary of the Haji-Gak Iron Area of Interest 463

iron ore deposits. A series of thrust faults have been mapped by Kusov and others (1965a,b) and are also 

indicated by the increased thickness of the iron ore and its host rocks within the central zone of the 

Haji-Gak iron orebody. A final phase of faulting consisted of the development of north-south and 

northwest-southeast faults that have offset the iron ores. Later post-Cretaceous extension led to the 

further development of northwest-southeast faults and graben structures that are filled with Quaternary 

to Recent sediment.

Figure 7A–10. Photograph of the Haji-Gak iron deposit looking northeast. The dark-colored outcrops (indicated 

by arrows) along the ridge line are the outcropping parts of the Haji-Gak iron orebody. Photograph by Will Stettner, 

U.S. Geological Survey.

Zones of contact metamorphism contain breccia zones near the orebodies that are dense and 

massive and contain local relict bedding. These breccia zones are highly fragmented and have 

micrometagranoblastic and microgranoblastic textures. These zones comprise quartz, iron hydroxide 

minerals, hydromica, and sericite, as well as local zoisite. Microquartz is common in many of the 

volcanic rocks, and mylonitization zones also are present as lenses of mylonitized and brecciated 

limestone that are up to 5 m thick along the base of plagioporphyrite and quartz plagioporphyrite in the 

Green Schist Formation.

7A.6 Structural Geology

The rocks of the Haji-Gak iron ore deposit form a large horizontally extended monocline, which 

coincides with the south limb of the larger Khoh-e-Baba anticlinorium. The rocks strike northeast and 

dip southeast (azimuth from 120° to 170°, angle from 35° to 80°). The monocline also contains smaller 

folds and fractures. The orebodies are conformable with layering of the host rocks. The Haji-Gak iron 

ore field has been divided into three northeast structural zones by Kusov and others (1965b)—the 

northern, middle, and southern zones. 
464 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

Figure 7A–11. Stratigraphic column of the Haji-Gak iron deposit area. Drafted from data from Kusov and others 

(1965b).

The northern structure zone contains cyclically repeated interbedded layers of schist with fine- to 

medium-textured phyllite as well as local interlayers of siliceous limestone (Kab Formation).Formation 

This zone is monoclinal and contains southeast dips (azimuth from 110° to 170°, dip angle from 35° to 

60°). In addition, this zone contains small-scale isoclinal, locally recumbent folds. Faults in the northern 

structure zone are brittle, but flow cleavage and shear zones are parallel to the schistocity.

The middle structural zone consists of the Awband and Green Schist Formations. The northern 

border of this zone coincides with the contact between the Awband and Kab Formations, and orebodies 

I, IX, and XII are located along this locally faulted contact. The southern contact of the middle structural 

zone passes along the Haji-Gak-Kharzar Fault. This zone comprises rocks having contrasting physical 

characteristics, including iron ore, various schists, sericite quartzite, marble, volcanic rocks, and alkaline 

rocks. These mixed physical properties played a major role in intense dislocation in this section 

compared with that of other sections. The middle structural zone is also monoclinal with the steep 

southeast dips (50° to 80° southeast). Most secondary folding in the Haji-Gak iron district is present in 

this zone. There are small symmetric and asymmetric folds, overturned and recumbent with limbs with 

dip lengths that range from 20 to 200 m and extend along strike for between 200 and 600 m. Kink 

banding is present within the schist. The faulting in the middle structural zone is both mesoscopic and 

megascopic, and cleavage is well developed. Foliation and shearing are abundant in the middle 

structural zone, as are brittle faults. The iron orebodies are fractured parallel to cleavage. The banded ore 

is sheared and marked by flow cleavage parallel to the schistocity.
Chapter 7A. Summary of the Haji-Gak Iron Area of Interest 465

Figure 7A–12. Structural analysis of bedding and foliation of the Haji-Gak iron orebody from Renaud and others 

(2011a). (a) Contoured poles to bedding on equal area stereonets from 11 separate domains showing moderate 

plunges to the southeast. (b) Geologic map of the Haji-Gak iron ore deposit.
466 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

Figure 7A–13. Photographs of outcrops of the Haji-Gak sedimentary iron deposit in Bamyan and Wardak Provinces from Peters and others (2007). 

(a) Pathway along outcrops of iron ore. (b) Outcropping layers of iron ore along the crest of the main ridge at Haji-Gak. Photographs by Robert Bohannon, 

U.S. Geological Survey. 
Chapter 7A. Summary of the Haji-Gak Iron Area of Interest 467

Figure 7A–14. Photographs of the Haji-Gak iron deposit area. (a) North view of the massive magnetite deposit at Haji-Gak (Stop 2, 34.66288° N, 

68.06736° E). (b) Close-up of south-dipping fine-grained bedded and brecciated limestone at the contact with massive magnetite (GPS 34.66299° N, 

68.06770° E). (c) View looking NW of the contact between massive magnetite (right, north) and fine-grained limestone (west, south). (d) Close-up of 

limestone showing the brecciated character and small clusters of magnetite (black) within the breccia matrix. Photographs by Robert D. Tucker, 

U.S. Geological Survey.
468 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

Figure 7A–15. Geology and cross-sections of the western parts of the Haji-Gak main iron orebody, modified from Kusov and others (1965a).
Chapter 7A. Summary of the Haji-Gak Iron Area of Interest 469

Figure 7A–16. Geologic map showing faults described in this chapter of this report and listed in table 7A–1 

(indicated by letters in circles). From Renaud and others (2011a).

The southern structural zone is confined to the Haji-Gak Formation. These rocks are deformed, 

especially near faults, but not as deformed as the rocks in the middle structural zone. Overturned folds 

are prominent near the Haji-Gak-Kharzar Fault. The carbonated rocks of this zone were fractured and 

contain horsetail fractures. Rocks near cross faults dip to the northwest (azimuth from 315° to 340°, 
470 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

angle from 80° to 90°), but movement is scissor-like because, along the southern part of the cross-fault,

the dip of the rock changes to the southwest with an azimuth of 130° to 160° and angles of 50° to 70°.

Kharzar Formation rocks are located to the south of the southern section. This flyschoid unit 

comprises clayey and sandy schists with interlayers of sandstones and microquartz. This unit has a 

monoclinal dip to the southeast and angles from 40° to 70° with weak secondary folding.

Faults in the Haji-Gak iron ore deposit field are transverse and diagonal and occasionally parallel 

to the bedding and schistocity. The size and movement of the faults varies from large to small strike-slip 

or dip-slip faults, thrust faults, and normal faults and shear zones along the cleavage. The biggest fault in 

this area is Haji-Gak-Kharzar followed by the following transverse and diagonal faults (listed by 

direction from west to east): Western I, II, and III, Naurak I and II, Khark, Lagernoye, Awband, Central, 

Sio-Sang, Chapkul I and II, and Eastern (fig. 7A–16; table 7A–22).

The Haji-Gak-Kharzar Fault extends 32 km along strike on a northeast bearing throughout the 

entire orebody and beyond (fig. 7A–16; table 7A–13). The Haji-Gak-Kharzar Fault is a thrust fault with 

displacement amplitude of between 700 and 1,000 m. Green Schist Formation rocks have been thrusted 

on top of the Haji-Gak rocks. On the surface, the Haji-Gak-Kharzar Fault displays an irregular 3-

to15-m-high fault scarp. Rocks along the fault are characterized by ductile deformation, fault rocks 

containing clay, and many slickensides on both walls of the fault. Schist and volcanic rocks near the 

fault are closely folded and mylonitized (fig. 7A–17).

Other major faults are the Western, Naurak, Kharh, Lagernoye, Awband, Central, Sio-Sang, 

Chapkul, and Eastern Faults (fig 7A–16; table 7A–2).) These faults are irregular transverse and diagonal 

and locally pass into horsetail morphology. The faults are left- or right-lateral or thrust faults, which 

offset the iron orebodies into blocks and displace them into steps or horsts and grabens (fig. 7A–16). 

These faults are brittle faults, having displacements of between 20 to 120 m horizontally and from 10 to 

50 m vertically. Along the Central Fault, the displacement is up to 1,400 m.

Slickensides, streaks, and furrows are common along on the surfaces of displaced blocks along 

the fault boundaries. Most of these fault structures are diagonally oriented between 40° and 50°. Some 

of the faults (Naurak, Western II, Central, and Chapkul) contain 2- to 10-m-wide fracture zones

(fig. 7A–16; table 7A–2).

The faults with the largest displacements are the Central and Chapkul II Faults, which break the 

iron ore field into three large blocks (fig. 7A–16; table 7A–2). Kusov and others (1965a) indicated that 

these faults predate the iron ore formation but that the orebodies in the three blocks were further broken 

into smaller blocks.

Lesser faults have formed in the ore. These are small faults that usually are splays of the larger 

faults. Normal faults are present in orebodies, on their contacts and in the host rocks. The displacement 

varies from 1 to a few meters mostly and in places can reach up to 10 m10 

Dikes and volcanic rock veins; quartz, barite, and calcite veinlets; and small hematite-magnetite 

ore veinlets are abundant in the Awband Formation host rocks and in the Green Schist Formation ore in 

the exocontact section of orebodies in the Kab Formation. These structures are mainly conformable and 

in places cross-cutting. Dikes are penetrated by hematite-magnetite ore veinlets. A few orebodies 

contain quartz veinlets and, in parts, quartz-carbonate and hematite veinlets. Orebodies in places do not 

have conformable contacts with the host rocks.

Kusov and others (1965b) suggest that much faulting occurred before ore formation, but that 

fractures and cleavage structures are present in all the orebodies and in all rocks that constitute the ore 

field.

There are four joint fracture systems according to Kusov and others (1965b). Most of joints 

strike northwest, as follows:

• azimuth dip from 175° to 215°, angle from 20° to 80°

• azimuth dip from 5° to 75°, angle from 70° to 90°

• azimuth dip from 115°to 155°, angle from 40° to 90°

• azimuth dip from 320°to 335°, angle from 80° to 90°
Chapter 7A. Summary of the Haji-Gak Iron Area of Interest 471

In places, foliation has the same attitude as the banding in iron ores, which is compatible with a 

volcanogenic origin for the ores. This similarity in attitude would imply that most of the faulting 

postdated the formation of the iron ores. However, there are indications that faults predated the 

formation of the iron ore in an epigenetic setting according to Kusov and others (1965b). These 

indications include the following:

• abundance of diabase dikes, which are conformable and in some places cutting (with cross-cutting 

veinlets, and in some parts with ore impregnations)

• the presence of small veinlets of ores, such as quartz-hematite-magnetite, quartz-magnetite and 

hematite-magnetite in Awband Formation schist

• the presence of parallel ore veinlets in diabase dikes along the contact of orebodies VII and IX

• filling the cutting contacts of host rocks by orebody materials with veinlets dispersion near salbands 

in host rocks

• the presence of brecciated structures in the iron ores, indicating the pre-ore fracture of marbles, 

derived from the Central and Chapkul II Faults as well as other faults

Small fractures in the iron ores owing to deformation show the same content as the primary 

content of orebodies. It is possible that some of these fractures formed by quartz-carbonate or 

quartz-carbonate-barite veinlets, which appear in orebodies.

Post-ore secondary faults identified by Kusov and others (1965b) are right- or left-lateral or 

normal-slip faults and thrust faults, such as the Western, Naurak, Kharh, Lagernoye, Awband, Sio-Sang, 

and Eastern Faults (fig. 7A–16; table 7A–2). These faults were followed by smaller scale faulting. The 

iron ore field was broken into step-like structures by these faults, and according to Kusov and others 

(1965b), horst and grabens were generated.

In general, Kusov and others (1965b) recognized that the Haji-Gak iron ore deposit is 

conformable with folded strata in the region and is confined to the limb of a monocline, which was 

folded again and fractured. The majority of orebodies are conformable with folded strata, but several of 

the orebodies cut folded strata. The main pre-ore folding was thought by Kusov and others (1965b) to be 

at the end of the Triassic and the beginning of the Jurassic during the Cymerian Orogeny. Post-ore 

folding probably occurred during Paleogene Alpine Orogeny. Both orogenic events would be post-ore 

with respect to a volcanogenic syngenesis of the iron orebodies.

There is tectonic activity taking place at the present time, which has resulted in the steep relief, 

intense erosion, steep slopes, and very high elevation. It is unlikely that weathering of the iron ores 

could have oxidized the ores in this environment.

7A.7 Alteration, Veining, and Mineralogy of the Haji-Gak Iron Ore Deposit

The mineralogy of the Haji-Gak iron ores varies throughout the deposit. The minerals in the iron 

deposit consist of ore and gangue minerals. The gangue minerals consist mainly of sulfide, carbonate, 

phosphate, and silicate minerals.

A number of hydrothermal alteration minerals are present within the Haji-Gak iron mineralized 

system. Hydrothermal alteration and metasomatism within the Haji-Gak iron deposit host rocks consist 

mainly of secondary sericite, which has microgranoblastic and local relict textures that develop into 

grey-colored zones that may be spotted, stratified, dense, or fragmental. Quartz and quartz-hematite 

veins contain sericite, hydromica, quartz, ore minerals, as well as chlorite, barite, apatite, sphene, and 

tourmaline. Carbonatization is marked by zones of grey, spotted, stratified, unsorted, granoblastic 

textured rocks comprising carbonate, quartz, ore minerals, sericite, and barite.
472 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

Table 7A–2. Features of faults of the Haji-Gak iron orebody.

[Kusov and others, 1965a,b. The faults are shown in figure 7A–16. M, meters; NA, not available] 

Fault letter Name of designation Type of fault Azimuth Dip Comments Displacement fault

on map

a Western I Left-lateral 220°–230° 85° Western wall displaced to 70 m.

the southeast, 

slickensides

b Western II Thrust fault 220°–230° 80° Eastern wall displaced and Horizontal 20 m, 

thrust, fractured vertical 15 m, 

displacement 

surface 25 m.

c Western III Thrust fault 230°–270° 80°–85° Western wall displaced and 16 m.

(irregular) thrusted, slickensides

d Naurak I Normal fault 250°–270° 75°–85° Western wall dropped Horizontal 10 m, 

down and displaced, vertical 7 m, 

friction surface 

displacement 13 m.

e Naurak II Normal fault 260°–270° 70°–80° Eastern wall dropped down Horizontal 10 to 40 m, 

and displaced, brecciated vertical 11 m, 

ore surface 

displacement 30 m.

f Kharh Thrust fault 270°–200° 75°–80° Western wall displaced to Horizontal 120 m, 

the south, friction vertical 50 to 55 m, 

surface 100 m.

g Lagernoye Left lateral 80°–90° 85° Western wall displaced to 20 m.

the south, 8 m wide

h Awband Right lateral 240° 85°–90° Eastern wall displaced 35 m.

i Central Thrust fault 200°–240° 75°–85° Western wall displaced, Surface 450 m, 

thrust under 45° horizontal 730 m.

j Sio-Jang Thrust fault 5°–10° 80° Northern wall displaced Surface 10 to 170 m.

and thrust, slickensides, 

breccia

k Chapkul I Normal fault 5°–10° 70° Northern wall displaced, 95 m.

friction

l Chapkul II Normal fault 50° 70° Western wall displaced Horizontal 350 m, 

vertical 70 m.

NA Eastern Thrust fault 40°–60° 80° Eastern wall displaced Horizontal 1,500 m, 

vertical 500 m.

Several different vein types are present in the Haji-Gak orebodies and in the surrounding host 

rocks. Post-magmatic veins and quartz veins are present in all rock types, but large veins are most 

common in sandy quartz-sericite slaty schist of the Kab Formation. The thickness of most veins is 1 to 

1.5 m, but some are as much as 10 to 50 m thick with dips between 30° and 90°. Magnetite-hematite 

veins are common in the orebodies, in diabase bodies, and especially in volcanic flows and schist of the 

Awband and Green Schist Formations. These veins have thicknesses of between 0.5 and 1 m and locally 

up to 5 m. Carbonate veins are prolific in Haji-Gak Formation. The highest density of carbonate veins is 

along the fractured zones. Barite is also present in veins and lenses near the orebodies among rocks of 

the Awband Formation and most commonly along fractured and faulted zones. The barite-rich vein 

thickness is between 0.1 and 0.5 m and locally up to 1 m. Locally, barite veins lie in clusters a few 

meters wide and 100 m long. 

Orebodies in the Awband Formation are divided into nonoxidized and semioxidized ores. 

Nonoxidized ores include pyrite-magnetite zones with high sulfur and magnesium concentrations 

(fig. 7A–18). The zones are massive (figs. 7A–13, 7A–14, and 7A–17), massive-banded, and spotted, 

containing mainly magnetite, hematite, pyrite, quartz, carbonate minerals, rarely chlorite, and sericite. 
Chapter 7A. Summary of the Haji-Gak Iron Area of Interest 473

Semioxidized ores comprise mainly hydrogoethite-semimartite, hydrogoethite-hematite-semimartite, 

and carbonate-semimartite. Hydrogoethite-semimartite and hydrogoethite-hematite-semimartite ores are 

fine- and medium-grained, massive, massive-banded, porous, and form veins and lenses that comprise 

mainly hydrogoethite, goethite, magnetite, martite, hematite, quartz, carbonate minerals, and pyrite. 

Carbonate-semimartite ores are massive, massive-banded, and spotted, and form veins and lenses that 

comprise magnetite, hematite, pyrite, quartz, carbonates, rarely chlorite, and sericite.

Figure 7A–17. Photographs of outcrops of the Haji-Gak sedimentary iron deposit in Bamyan and Wardak Provinces from 

Peters and others (2007). (a) Photograph showing iron deposit at the crest of ridge and foliated schist in the foreground.

(b) Photograph of joint U.S. Geological Survey-Afghanistan Geological Survey field reconnaissance team (2006)at 

exploration adit in iron ores of the Haji-Gak deposit. Photographs by Robert Bohannon, U.S. Geological Survey.
474 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

Figure 7A–18. Photographs of ores from the Haji-Gak iron ore deposit. (a) Photograph of hand specimen of 

mixed magnetite and semimartite iron ore. (b) Euhedral pyrite magnetite ore. Photographs from Afghanistan 

Geological Survey files (scale approximate). Photographs by the Afghanistan Ministry of Mines.

7A.8 Primary Nonoxidized Ores

The primary nonoxidized ores mainly are pyrite-magnetite ores. These pyrite-magnetite ores are 

present to a depth of 100 m, but are not well documented. The ores are dense, fractured, steel-black in 

color, and exhibit massive to banded and spotted textures with fine- to medium- and rare coarse-grained, 

xenomorphic (cathedral) and idiomorphic grains. The pyrite-magnetite ores mainly consist of iron 
(56.24 to 68.80 wt. %, averaging 61.30 wt. % iron). Bands in the ores show massive-banded textures and 

contain impregnations of pyrite and non-ore minerals, as well as altered magnetite and hematite bands. 

Spotted ores are present near the contacts of the ore with the host rock and are characterized by sporadic 

and uneven disseminations of pyrite, siderite, and quartz, as well as sparse barite, calcite, and dolomite 

impregnations (Kusov and others, 1965a) 

Ore minerals in the pyrite-magnetite ores are predominantly magnetite and pyrite, with rare 

hematite and martite. Magnetite is present as massive, xenomorphic masses with cataclastic textures. 

The content of magnetite in the pyrite-magnetite ore varies from 40 to 90 vol. % and the average content 

is 68 vol. % (figs. 7A–18 and 7A–19). Hematite is present as flakes between magnetite grains or in 

veins. The content of hematite in the pyrite-magnetite ores does not exceed 2 vol. %. Martite in the 

pyrite-magnetite ore is present as pseudomorphs (the edges of magnetite grains alter into martite), 

including pseudomorphed magnetite grains with pyrite inclusions. The content of martite does not 

exceed 5 vol. %. Siderite is an abundant mineral in pyrite-magnetite ores, especially along the ore-host 

rock contact. It is present as veins and veinlets that penetrate the magnetite masses. Siderite usually is 

adjacent to quartz and chlorite, and exhibits a fine-grained, granoblastic texture. The siderite content 

varies from 1 to 25 vol. % of the pyrite magnetite ore. 

Gangue minerals in primary nonoxidized ores include carbonate minerals (calcite, dolomite and 

siderite), silicate minerals (quartz, chlorite), sulfide minerals (chalcopyrite, pyrrhotite, barite, and 

pyrite), and phosphate minerals. Calcite and dolomite vary from 5 to 6 vol. % and are present as spots in 

quartz veins with quartz, pyrite, and barite. Quartz is the most abundant non-ore mineral in the Haji-Gak 

iron deposits. It is present in three generations and comprises between 6 and 10 vol. % of the ores. The 

first generation of quartz formed almost simultaneously with magnetite. The second generation of quartz 

formed after magnetite and almost simultaneously with hematite. The third generation of quartz formed 

along with sulfide minerals and forms accumulations from 0.1 to between 10 and 30 centimeters (cm) 

thick. Early third generation quartz also contains pyrite inclusions. Late third generation quartz is 

adjacent to calcite, dolomite, and barite. Chlorite is present in banded textures with quartz, calcite, and 

barite. The chlorite content of most ores is 1 vol. %. 

Pyrite crystals [0.01 to 5 millimeters (mm) in diameter] are unevenly disseminated throughout 

the primary nonoxidized iron orebodies (fig. 7A–19a) and also form dense impregnation bands; the 

content of pyrite averages 14 vol. % in the ores. Barite is sporadically dispersed throughout the pyritemagnetite ore and makes up 2 vol. % of the ore. Barite is usually spatially adjacent to quartz and 

carbonate minerals and locally with pyrite; fills voids between quartz, pyrite, and magnetite grains; and 

forms veins and veinlets. Chalcopyrite (less than 0.2 mm in diameter) and pyrrhotite (up to 0.07 mm in 

diameter) also are rarely present with pyrite and siderite as inclusions, and these sulfide minerals 

combined constitute 1 vol. %. 

The pyrite-magnetite ores require desulphurization and agglomeration and further metallurgical 

processing. Metallurgically harmful mineral mixtures in the ores are sulfur (sulfatic and sulfidic

minerals, 4.75 wt. %),% phosphorus (0.05 wt. %), and zinc (less than 0.01 wt. %). The sulfidic sulfur 

occurs with barite, and its content is 0.04 wt. %. The sulfidic sulfur occurs with pyrite, and its content is 

4.69 wt. %. Metallurgically nonharmful mineral mixtures in the ore are nickel 0.001 to 0.01 wt. %), 

copper 0.003 to 0.01 wt. %), cobalt trace amounts to 0.001 wt. %), silver (trace amounts), and 

manganese (trace amounts). Barium (0.001 to 0.06 wt. %) is present as barite. 

7A.9 Primary Semioxidized Ores

Primary semioxidized orebodies contain hydrogoethite-semimartite, hydrogoethite-hematitesemimartite, and carbonate-semimartite ores. Tables 7A –3 and 7A –4 list the descriptions and mineral 

contents of primary semioxidized ores. 

Chapter 7A. Summary of the Haji-Gak Iron Area of Interest 475
476 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

7A.9.1 Hydrogoethite-Semimartite Ores

Hydrogoethite-semimartite ores are predominant in the Haji-Gak iron deposit and extend from 

the surface to between 100 and 130 m deep. They are dense, steel-black in color with brownish tints, 

fine to medium-grained, xenomorphic, with massive-banding, and in places have spotted textures 

(fig. 7A–20c). The hydrogoethite-semimartite ores also display porous textures, which are most likely 

owing to leaching of nonmetallic minerals and to pyrite oxidation. The tops of the pores usually are 

covered with rims of hydroferric oxide minerals and carbonate minerals. The content of ore in 

hydrogoethite-semimartite orebodies is 52.29 to 68.32 vol. %, with an average content of 62.32 vol. %. 

Ore minerals of the hydrogoethite-semimartite ore include magnetite-martite, goethite, hydrogoethite, 

and magnetite.

Figure 7A–19. Photographs of pyrite-magnetite ores of Haji-Gak iron deposit from Kusov and others (1965b). 

(a) Pyrite-magnetite ore with massive-banded texture, comprising ground mass, the thin bands formed by siderite 

and pyrite; from core hole 2 at a depth of 148 meters. The white spot at the bottom is quartzite. (b) Pyrite-magnetite 

ore with spotted texture. Magnetite is black, siderite is white, and pyrite is grey. Sample is from core hole 1 at a

depth of 125.9 meters. (c) Magnetite that exhibits xenomorphic, coarse-grained texture and shows cataclasis; from 

thin section 150-I.
Table 7A–3. Description and mineral content of ore. [Kusov and others, 1965a,b. All values are in percent. Ag, silver; Ba, barium content; BaCo3, barium; Co, cobalt; Cu, copper; Ni, nickel; NA, not available; 

P4, phosphorus ; V, vanadium; Zn, zinc; —, zero; <, less than] 

Primary nonoxidized, pyriteMineral magnetite ore Hydrogoethite se

Range Average Range

Primary semioxidized

mimartite ore Hydrogoethite hematite semimartite or

Average Range Average

e Carbonate semimartite ore

Range Average

Ore minerals

Magnetite 40–90 68 5–70 39 1–47 31 20–60 39

Pyrite 2–35 14 0–5 <5 0–6 — 0–10 2 

Siderite 1–25 8 single grains — — — 2–30 5 

Hematite 0–2 <2 0–20 5 10–50 33 — — 

Martite 0–5 <5 1–80 20 2–55 19 1–18 10

Hydrogoethite — — 1–85 25 1–20 10 1–5 3 

Chalcopyrite single grains — — — — — — — 

Muscovite — — single grains — — — — — 

Maghemite — — single grains — — — — — 

Pyrrhotite single grains — — — — — — — 

Non-ore minerals

Quartz 1–10 6 1–25 7.5 1–8 4 0–8 3 

Dolomite 1–6 2 0–2 1 0–2 — 15–50 28

Calcite 1–5 1 0–3 — NA NA 5–20 7 

Chlorite 0–9 <1 0–5 — 0.5–8 — — — 

Sericite — — 0–2 — 0–2 — — — 

Ankerite — — single grains — — — — — 

Actinolite — — single grains NA 0–1 — — — 

Plagioclase — — single grains — 0–3 — — — 

Gypsum — — 0–5 — single grains — — — 

Magnesite — — single grains — — — — — 

Talc NA NA NA NA single grains — — — 

Barite 0–2 2 0–3 — single grains — NA NA

Harmful mixture

Sulfatic (barite) 0.04 NA 0.04–1.97 0.11 NA NA 0.06 NA

Sulfidic (pyrite) 4.69 NA NA NA 0.07 — NA NA

P4 0.05 NA 0.02–0.09 — 0.046 — 0.05 NA

Zn <0.01 NA < 0.01 NA NA — 0.01 NA

Good mixture

Ni 0.001–0.01 NA 0.03–0.02 NA 0.001 — trace-0.003 NA

V — NA NA NA 0.001 — trace-0.003 NA

Cu 0.003–0.01 NA trace-0.01 NA 0.001 — traces NA

Co trace-0.001 NA 0.002–0.005 NA 0.001 — trace-0.01 NA

Ag traces NA NA NA — — — — 

Mn traces NA NA NA — — — — 

Chapter 7A. Summary of the Haji-Gak Iron Area of Interest 477
478 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

Primary nonoxidized, pyrite- Primary semioxidized

Mineral magnetite ore Hydrogoethite semimartite ore Hydrogoethite hematite semimartite ore

Range Average Range Average Range Average

BaCo3 (Ba) 0.001–0.06 NA NA NA 0.01–0.06 0.02

Table 7A–4. Description and mineral content of ore, showing grain size.

[Kusov and others, 1965a,b. Values are in millimeters. NA, not available; —, zero]

Primary nonoxidized, pyrite- Primary semioxidized

Mineral magnetite ore Hydrogoethite semimartite ore Hydrogoethite hematite semimartite ore

Range Average Range Average Range Average

Ore minerals

Magnetite 0.01–1 0.2 0.01–4 0.2 0.01–3 0.3

Carbonate semimartite ore

Range Average

— —

Carbonate semimartite ore

Range Average

0.02–4 0.3

Pyrite 0.1–5 0.3 as large as 4 — 0.01–0.4 0.2 0.1–4.5 0.3

Siderite 0.1–4 0.2 as large as 4 — — — 0.2–4 0.5

Hematite as large as 3 — as large as 5 — 0.1–6 0.5 — —

Martite as large as 0.2 — 0.01–1 0.2 0.01–0.2 0.1 0.01–3 0.1

Hydrogoethite — — 0.01–0.5 0.4 0.01–0.5 0.2 0.1–0.3 0.2

Chalcopyrite as large as 0.2 — — — — — — —

Muscovite — — as large as 1 — — — — —

Maghemite — — as large as 1 — — — — —

Pyrrhotite as large as 0.07 — — — — —

Non-ore minerals

Quartz 0.01–1 0.3 as large as 5 0.15 0.01–0.1 0.05

— —

0.01–0.5 0.1

Dolomite 0.2–5 0.5 0.2–5 2 0.2–5 0.4 0.02–6 0.3

Calcite as large as 5 0.3 0.1–6 0.3 NA NA 0.05–4 0.3

Chlorite as large as 5 — as large as 1 — 0.5–2 0.4 — —

Sericite — — as large as 1 — as large as 0.2 — — —

Ankerite — — as large as 2 — — — — —

Actinolite — — as large as 3 NA 0.1–2 0.5 — —

Plagioclase — — as large as 5 — 0.3–9 0.1 — —

Gypsum — — 0.2–6 0.5 as large as 5 — — —

Magnesite — — as large as 2 — — — — —

Talc NA NA — — as large as 0.2 — — —

Barite as large as 0.5 — 0.1–0.3 0.5 as large as 0.2 — NA NA
Chapter 7A. Summary of the Haji-Gak Iron Area of Interest 479

Hydrogoethite-semimartite ore formed as a result of supergene processes on pyrite-magnetite 

ores (Kusov and others, 1965b). Magnetite is the predominant mineral in hydrogoethite-semimartite 

orebodies, and its content varies from 1 to 70 vol. %, with an average of 39 vol. %. The characteristic 

grain size and structures are similar to the magnetite in pyrite-magnetite ores. Magnetite grains display 

three main types of texture. The first is xenoblastic where magnetite grew during metamorphism without 

developing crystal faces (fig. 7A–20c). The second texture is hypidioblastic, where newly formed 

subhedral crystals are bounded in part by characteristic crystal faces (figs. 7A–18 and 7A–20a). The 

third texture is recrystallization near the fault zones (fig. 7A–20b

• rims that develop along pseudomorph cleavage planes and fractures within magnetite grains; during

intensive replacement, the rims form a web or acquire a spongy texture 

). Martite is a hematite pseudomorph of 

magnetite that constitutes 1 to 80 vol. % of the orebody and is unevenly disseminated throughout the 

ore. The martite has the following forms: 

• replacing magnetite along cracks or forming rims along the magnetite edges, creating a mesh texture

• forming small spotted grains with zoned rims

• pseudomorphing magnetite either along cracks or entire magnetite grains 

Iron hydroxide minerals (mainly hydrogoethite) are well developed and dispersed in the 

oxidation zone. The content of iron hydroxides in ore is 85 vol. %,with an average content of 25 vol. %. 

Iron hydroxide minerals formed from oxidation of magnetite, pyrite, siderite, and partially martite (the 

process of magnetite replacement by iron hydroxides is more intensive than martitization). Hydroxides 

replace magnetite in different ways, such as accumulations or webs (fig. 7A–21b

Gangue minerals in the hydrogoethite-semimartite ores include silicate (mica, quartz, talc, 

plagioclase, zircon, and actinolite), sulfide (pyrite), and carbonate (siderite, carbonate) minerals. Quartz 

is the predominant non-ore mineral and occurs in three generations within hydrogoethite-semimartite 

ore, as in the pyrite-magnetite ores in spotted forms or veins. Muscovite forms sheets in the groundmass 

of orebody I with isometric magnetite grains and was developed during the formation of hematite and 

the sulfidic mineralized zones. Talc and gypsum also are secondary minerals in hydrogoethitesemimartite ores. Plagioclase and actinolite are remnant minerals in the ores. Zircon is a very sparse 

mineral in the orebodies. Pyrite in primary semioxidized ores is present as impregnations and relicts that 

are unevenly dispersed within the host rocks. The content of pyrite in the iron ores does not exceed 

5 vol. %, and the mineral is absent in ores that are at a depth greater than 50 to 80 m. Carbonate minerals 

are also remnants within the ore.

). Hematite is dispersed 

unevenly and comprises 20 vol. % of ore, with an average of 5 vol. %. Hematite in massive ores fills 

voids between magnetite grains and also forms veins and veinlets. In banded ores, hematite forms 

0.5-mm-thick sheets. Hematite formed in two generations. The first was subsequent to magnetite and 

formed banded accumulations and inclusions among magnetite grains. The second is characterized by 

monomineralic veins with quartz. Siderite developed near the orebody contact with dolomitic marble 

and schist. Siderite has been oxidized into iron oxide minerals that occur in single grains or in 

accumulations between magnetite grains.

Metallurgically harmful elemental mixtures in the hydrogoethite-semimartite ores include sulfur, 

phosphorus, and zinc (Kusov and others, 1965b). Sulfur is highly abundant with concentrations from 

0.04 to 1.97 wt. %, with an average of 0.11 wt. %, and is present as sulfatic (barite and gypsum) and 

sulfidic (pyrite) sulfur. The content of sulfur in sulfatic sulfur does not exceed 0.04 wt. %. Phosphorus 

appears in isomorphous mixtures, with a concentration that varies from 0.02 to 0.09 wt. %. Zinc 

concentration in ores usually does not exceed 0.01 wt.%. Metallurgically useful elemental mixtures are 

manganese, nickel (0.03 to 0.02 wt. %), cobalt (0.002 to 0.005 wt. %), copper (trace to 0.01 vol. %), 

silver, and barium. 
480 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

Figure 7A–20. Photographs of hydrogoethite-semimartite ore from Kusov and others (1965b); scale not recorded. 

(a) Hydrogoethite-semimartite ore with massive hypidioblastic texture. Magnetite (dark grey) underwent

martitization (light-grey) and developed pores (black); from thin section 1638-I. (b) Hydrogoethite-semimartite ore 

that has been recrystallized. Magnetite (grey) includes quartz (dark grey); from thin section 454-I. (c) Hydrogoethitesemimartite ore with massive texture. Pores (black) are superjacent; magnetite (light-grey) grains illustrate 

xenoblastic texture; from thin section 454-I.

7A.9.2 Hydrogoethite-Hematite-Semimartite Ores

Hydrogoethite-hematite-semimartite ores are not abundant in the Haji-Gak iron deposit. They are 

fine- to medium-grained banded ores that are dense and steel-black in color (fig. 7A–22). Vugs are 

dispersed unevenly and range in size from 0.1 to 5 mm in diameter. The iron content varies from 59.49 

to 65.68 wt. %,with an average of 62.66 wt. %. The hydrogoethite-hematite-semimartite ores are present 

as lenses (25.5 m thick from surface and 340 to 650 m long along the strike). Hydrogoethite-hematitesemimartite ores are similar to hydrogoethite-semimartite ores, and during the estimation of ore 

reserves, both ores were considered to be a single commercial ore type (table 7A–1). The only difference 

between the two ores is a higher concentration of hematite and banded textures in the hydrogoethitehematite-semimartite ore (fig. 7A–22). These ores are present in oxidized zones at depths between 100 

and 130 m from the surface. 
Chapter 7A. Summary of the Haji-Gak Iron Area of Interest 481

Ore minerals in the hydrogoethite-hematite-semimartite ores include magnetite, hematite, 

martite, and hydrogoethite (Kusov and others, 1965b). Magnetite (with a grain size from 0.01 to 3 mm 

in diameter) content is 1 to 47 vol. %; hematite (with a grain size from 0.1 to 6 mm in diameter) content 

is 10 to 50 vol. %; martite (with a grain size from 0.01 to 0.1 mm in diameter) content is 2 to 55 vol. %; 

and hydrogoethite (with a grain size from 0.01 to 0.2 mm in diameter), content is 1 to 20 vol. %. 

Gangue minerals include silicate (quartz, chlorite, plagioclase, actinolite, talc, and sericite), 

carbonate (carbonate and dolomite), and sulfide and sulfate (barite, gypsum, and pyrite) minerals. 

Metallurgically harmful elemental mixtures in the hydrogoethite-hematite-semimartite ores are sulfur 

and phosphorus. The sulfur content is 0.07 wt. %, and the phosphorous content is 0.046 wt. %. 

Metallurgically useful elemental mixtures in the hydrogoethite-hematite-semimartite ores are nickel, 

vanadium, copper, and cobalt. The content of each element does not exceed 0.001 wt. %. Barium was 

identified at 0.01 to 0.06 wt. %, with an average of 0.02 wt. %. 

Figure 7A–21. Photographs of martite-bearing ores from Kusov and others (1965b); scale not recorded. 

(a) Martite (light grey)replaces magnetite (dark grey), creating a web or spongy texture. Dark-grey loops are iron 

oxide minerals, and areas in black are the pores and quartz. From thin section 1733. (b) Photograph of martite 

(white) replacing magnetite (grey), creating a mesh texture. Black is pores, and dark grey is the iron oxide minerals. 

From thin section 3g.

7A.9.3 Carbonate-Semimartite Ore

Carbonate-semimartite ore is less abundant than the other ores and occurs along the transitional 

zone between hydrogoethite-semimartite and iron ores in dolomitic marble and dolomitic limestone. 

Carbonate-semimartite ore is dense, mainly spotted (fig. 7A–23a), with a banded texture (fig. 7A–23b), 

and fine- to coarse-grained. The bands of the ore comprise magnetite and dolomite.

Ore minerals in the carbonate-semimartite ores include magnetite, martite, siderite, and 

hydrogoethite. Gangue minerals include silicate, such as sparse quartz; carbonates, such as dolomite and 

calcite; and sulfides, such as pyrite (Kusov and others, 1965b). Metallurgically harmful elemental 

mixtures include sulfur, phosphorus, and zinc. The content of these components is very low; sulfur 

content is 0.06 wt. %, phosphorus content is 0.05 wt. %, and zinc content is 0.01 wt. %. Metallurgically

useful elemental mixtures in the carbonate-semimartite ores include nickel (trace amounts to 

0.003 wt. %), vanadium (trace amounts to 0.003 wt. %), copper (trace amounts), and cobalt (trace 

amounts to 0.01 wt. %). A carbon dioxide content of 13.35 wt. % was also determined.
482 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

7A.9.4 Fragmental Ore

Fragmental ores are represented by a single industrial type of ore, hydrogoethite-semimartite ore. 

Fragmental ores are present as talus in loamy sand and as ore fragments and rubbles of quartz, schist, 

and dolomitic marble. The ore fragments are present as boulders, colluvial rubble, and in places as 

subrounded cobbles of hydrogoethite-semimartite, hydrogoethite-hematite-semimartite, and 

carbonate-semimartite ores. Fragmental ores are rich in iron. Metallurgically harmful elemental mixtures 

in the fragmental ores include sulfur and phosphorus. The content of these components is very low and it 

does not impact the ore quality. Metallurgically useful elemental mixtures include nickel, vanadium, 

copper, and cobalt. The total content of useful elemental mixtures is approximately 0.01 wt. %. 

Figure 7A–22. Photograph of hydrogoethite-hematite-semimartite ore with banded texture from Kusov and others 

(1965b). The light grey bands are hematite, and the dark grey bands are martitized magnetite from sample 6, adit 1.

Figure 7A–23. Photographs of carbonate-semimartite ore with banded texture from Kusov and others (1965b); 

scale not recorded. (a) Photograph of carbonate-semimartite ore with banded texture, showing dolomite (white) and 

altered magnetite (black); sample K-12-1. (b) Carbonate-semimartite ore with spotted texture; marble (white) and 

martitized magnetite (black); sample K-12-2.

7A.10 Genesis of the Haji-Gak Iron Ores

A genetic model of the Haji-Gak iron deposit was proposed by Kusov and others (1965b). It is an 

epigenetic model derived from observations made on the geologic host rock and the inferred 

environment of deposition. The iron ore deposits of the Haji-Gak iron deposit are hosted by the 

Neoproterozoic(?) Awband Formation, which comprises sericite and quartz-sericite schist, 

quartz-sericite schist (derived from acidic tuff), carbonate-chlorite-sericite schist (derived from tuff), 
Chapter 7A. Summary of the Haji-Gak Iron Area of Interest 483

marble, and dolostone. The Awband Formation rocks have been folded, faulted, and intruded by 

diabase. The ore in the Haji-Gak iron deposit area is controlled by stratigraphy and structure. 

Structural and stratigraphic control of the Haji-Gak iron deposit and other peripheral areas of the 

iron ore were thought by Kusov and others (1965b) to be owing to the proximity of the Haji-GakKharzar regional deep fault zone. Therefore, the ores were thought to be spatially and genetically related 

to small plagiogranite, granodiorite, and quartz diorite intrusive bodies, which also are located along the 

same fault zone as the iron deposits. The ores and the intrusive bodies were proposed as products from 

the same magma source but formed at different times. The regional fault and fault splays were 

hypothesized to be the channels for the intrusive bodies (silicate melts) and for the migration of the iron 

ore solutions. The orebody shape was caused by alteration of favorable rocks (schist derived from tuff, 

dolomitic limestone, and marls) or by ore precipitation in the open cracks. These suppositions are 

compatible with processes that take place during volcanogenic ore genesis also.

The contact between the iron orebodies and host rocks locally produced remnants of host rocks 

contained within the orebodies. The sharp and straight contact between host rocks (sandy quartz-sericite 

schist and sericite quartzite) and iron orebodies were thought by Kusov and others (1965b) to be formed 

by differences in permeability of the host rocks. The sharp and straight cross-cutting orebodies (IX, 

XIII; fig. 7A–24b

Change in the footwall of ore host rocks was thought by Kusov and others (1965b) to be owing 

to alteration near the orebodies from the introduction of quartz and sericite and replacement of the host 

rocks rather than by syngenetic processes. Propylitization and carbonation were also thought to have 

taken place distal from the orebodies forming metasomatic carbonatite.

) indicated the formation of orebodies in open spaces. Gradational, irregular, and wavy 

contacts of orebodies (I, IX; fig. 7A–24) with marl, dolomitic limestone, and schist (derived from tuff) 

indicate metasomatic replacement of the host rocks by the iron ore. Iron orebodies contain remnants of 

host rocks, such as schist with thin iron ore veins, which have been altered into sericitic quartzite during 

hydrothermal processes. The schistose texture of these remnants coincides with banded ore and retains 

the same spatial orientation as the host rocks (figs. 7A–15 and 7A–24). These observations also are 

compatible with processes that are coeval with volcanism.

Mineralogical, geochemical, petrographical, textural, and structural genetic criteria of the iron 

ores were thought by Kusov and others (1965b) to be marked locally by massive, banded, and spotted 

textures, but mainly by fine- and medium-grained textures, as well as by sandy and occasionally 

hypidiomorphic textures. Banded textures in the ores mainly are present parallel to the schistosity and 

represent replaced schistose host rocks, whereas replacement massive textures are likely to be present in 

carbonate rocks. These textures also are compatible with volcanogenic and syngenetic processes. Relict 

minerals and textures interpreted to be from incomplete replacement by Kusov and others (1965b) may 

also be owing to syngenetic processes. The remnants (relicts) of actinolite, sericite, and chlorite were 

preserved in banded ores, which occur during alteration of schists, and carbonate relicts and local 

pseudomorphs of magnetite along the rhombs of dolomitization were preserved in massive ores. 

The paragenetic sequence of minerals in primary nonoxidized ore is magnetite, muscovite, 

hematite, quartz, pyrite, siderite, albite-oligioclase, barite, actinolite, and chlorite. The presence of 

associated element mixtures in ore, such as nickel, copper, barium, vanadium, zinc, and sometimes 

cobalt, silver, and molybdenum, in combinations with primary iron, silica, potassium, carbon dioxide, 

and sulfur, also indicates hydrothermal ore-bearing solutions were involved in ore genesis. The weakly 

expressed, vertical primary zonation of orebodies, caused by high concentrations of ore sulfide minerals 

(mainly pyrite) and copper (as chalcopyrite) at a depth of 100 to 130 m and the low concentration of 

hematite, was thought by Kusov and others (1965b) to indicate hydrothermal endogenic ore formation; 

however, the same zonation of orebodies can also be accounted for by folding or metasomatic reworking 

of stratabound, syngenetic orebodies. 
484 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

Figure 7A–24. Photographs of Haji-Gak iron ores showing layering from Kusov and others (1965b). (a) Remnants 

of sericite quartz in ore; from shaft # 1 at an interval of 180 to 189 meters. (b) Remnants of sericite quartz (light) 

among hydrogoethite-semimartite ore (black); the contact of hydrogoethite-semimartite ores with carbonate-chloritesericite schist is shown. 

The source of ore-bearing epigenetic solutions was postulated by Kusov and others (1965b) to be 

a deep magmatic center. The product of this hypothetical magmatic center was also thought to have 

undergone magmatic distillation with separation into silicate melt and a gas phase. The intrusive bodies 

were speculated to be the small intrusions of plagiogranite, granodiorite, quartz diorite and 

hydrothermal-metasomatic mineralization (ore veins, barite veins, metasomatic carbonatite, and 

alteration of footwall rocks). These intrusive bodies, along with co-magmatic volcanic rocks found at 

Haji-Gak are also typical of volcanogenic environments. The hydrothermal ore-bearing solutions were 

formed from gas phases. Kusov and others (1965b) thought that the primary components of geochemical 

hydrothermal solutions, based on the footwall alterations, are Fe, Si, Ca, K, carbon dioxide, sulfuric 
Chapter 7A. Summary of the Haji-Gak Iron Area of Interest 485

acid, Ba, and Mg, followed by Na, Zn, Ni, Cu, V, Co, Ag, and Mo, indicating a process by which the 

formation of hydrothermal solutions evolved as a gas that migrated into the host rocks, followed by the 

alteration of the host rocks and cooling that led to transition into the liquid phase.

The main ore host structures were interpreted by Kusov and others (1965b) to be the Haji-GakKharzar fault that splayed from the main faults followed by folding and intensive fracturing. Rather than 

postdating syngenetic ore, these structural zones were thought to serve as ore-bearing solution pathways 

from a magmatic center to sites of ore precipitation. Furthermore, the contact between the heterogeneous 

Awband Formation and the relatively homogeneous Kab Formation was faulted prior to ore formation 

and the footwall of the ore zone lies along this contact. Therefore, the Kab Formation rocks are 

interpreted by Kusov and others (1965b) to have served as an impermeable barrier during ore formation.

Beds and lenses of marl, dolomitic limestone, and carbonate-chlorite-sericite schist (derived 

from tuff) are interpreted by Kusov and others (1965b) to be thoroughly replaced by iron ores, such that 

small beds are located between impermeable rocks or partially permeable rocks and thick beds and were 

not limited in permeability (orebodies I, and IX, fig. 7A–25b

“Orebodies VII and XIII coincide with longitudinal folded structures or cross-cutting faults, which 

were formed before ore formed. Faulted and folded structures, in the areas of unfavorable for 

replacement of rocks, such as sericite quartzite, quartz-sericite schist, alkaline volcanic rocks, 

plagiogranite, granodiorite, and quartz diorite, coincide with small quartz-hematite veinlets and 

veins. The veinlets and veins in dolomitic limestone marl and carbonate-chlorite-sericite schist 

served as a path for migration and interoperability of ore-bearing solutions with indicated rocks. 

Fractures formed before ore deposition allowed the circulation of ore-bearing solutions and formed 

favorable conditions for permeability within the host rock that underwent replacement.”

). Further interpretation of the epigenesis of 

the orebodies by Kusov and others (1965b) is as follows:

Epigenetic interpretations of ore formation by Kusov and others (1965b) are that hypogene ore 

genesis took place in three stages. The first stage is marked by dolomitization, silicification of the host 

rocks, and precipitation of magnetite, hematite (iron mica), and quartz and involves deposition of 

magnetite with quartz and deposition of magnetite-hematite. The second stage of mineralization is 

characterized by carbonatization, sericitization of the host rocks, and the deposition of hematite, pyrite 

with quartz, siderite, and barite. During this phase, barite inclusions formed in the iron ores and veinlets 

of hematite with quartz grew in massive sulfide-rich (mainly pyrite) areas. The first two stages constitute 

the main ore-forming stages. The third phase involves the formation of veins, veinlets, siderite

inclusions, and occasionally pyrite with quartz and barite with carbonate minerals and quartz. During the 

third phase, the ore-bearing solutions were not enriched in iron, and as a result, during interaction with 

the host rocks, such as limestone and dolomite, siderite was formed. The high content of sulfide 

minerals (mainly pyrite) indicates a nonoxidized environment. The deposit was thought to have formed 

at moderate depths under moderate temperatures as indicated by the ore mineralogy, the spatial 

connection of ore with the intrusive bodies, and the ore structures.

A final supergene overprinting stage of ore formation converted the nonoxidized pyritemagnetite ore with hematite and siderite into semimartite and in places into martite ores containing iron 

hydroxide minerals. The alteration of the mineral content was considered by Kusov and others (1965b) 

to be mainly by oxidation of ore minerals and also by partial decomposition of non-ore minerals. 

Maghemite, martite, goethite, and hydrogoethite were derived from primary ore minerals. Magnetite was 

partially replaced by supergene hematite (martite). Locally, martite was oxidized to goethite and 

hydrogoethite. Frequently, magnetite was oxidized to iron hydroxides, and locally magnetite was altered 

to maghemite. Primary hematite was altered. Pyrite was thoroughly oxidized, and left behind iron ochre 

in pores after the leaching process. Carbonate minerals, quartz, and magnesium were leached and 

siderite was oxidized to residual iron hydroxide minerals.

Quartz, chlorite, sericite, and some other minerals in the supergene ores are typical residual 

products. The main change of physical properties in the supergene ores is the development of porous 
486 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

textures. As a result of pyrite oxidation and of partial leaching of the non-ore minerals the ores became 

enriched in iron. 

Although mesoscopic textures indicate hydrothermal-metasomatic conditions during the 

formation of the Haji-Gak iron deposit, the genesis of the deposit is not well understood. The main 

reason is that the primary ore’s relations among host rocks at depth have not been well studied. 

The age of the Haji-Gak iron deposit, based on tectonic, magmatic, and stratigraphic conditions 

known in the area, was thought to be Early Jurassic by Kusov and others (1965b), who based this 

interpretation on the spatial association of the ores with tectonic and magmatic processes that are 

thought to be Early Jurassic. The volcanic rocks, plagiogranite, granodiorite, and quartz diorite contain 

cross-cutting veins and veinlets, as well as hematite inclusions, magnetite, or hematite-magnetite-quartz. 

Orebodies VI and XI (fig.7A–25b) cut granodiorite and plagiogranorite dikes. Taking into consideration 

the connection of ore and intrusions with one magmatic center, the time of their formation is 

synchronized. Metamorphism of the ore was thought by Kusov and others (1965b) to be absent, whereas 

some host rocks such as the Devonian and Cretaceous ages were not considered metamorphosed. The 

connection of ore formation with fractured structures of post-Devonian age indicated to Kusov and 

others (1965b) that the Haji-Gak iron deposit was of Early Jurassic age. 

7A.11 Ore Reserve Estimation and Reserves and Resources

In 1963 and 1964, the Afghanistan Geological Survey Russian contractor measured and 

estimated the iron resource of the Haji-Gak iron deposit. The western part of the Haji-Gak area was 

intensively explored, while the central and eastern parts were explored less. 

This exploration work included making maps at a scale of 1:50,000 and 1:10,000, drilling holes, 

and digging trenches, adits, and shafts. Samples were collected, and prospect lines (traverses) were 

drawn. The data collected from trenches, shafts, and prospect lines were used to create vertical cross 

sections and horizontal plans, which were then used to calculate the end areas of the geometrical figures

and then used to calculate the volume of the ore. 

Primary ores are subdivided into 16 orebodies that have been designated by Kusov and others 

(1965a,b) by roman numerals I through XVI (fig. 7A–25). Fragmental ores are subdivided into four 

orebodies (A, B, C, and D; fig. 7A–25). The natural ores were further subdivided into resource 

categories A, B, C1, and C2, and separate plans were drawn for the orebody that was explored. The 

calculated tonnages for the reserves and resources are listed in tablet 7A–5. 

7A.11.1 Prospects and Anomalies

A number of non-iron deposits, prospects, and occurrences are present in the Haji-Gak iron 

deposit and adjacent subareas. Known prospects and anomalies are the Haji-Gak barite, Haji-Gak 

limestone, and Haji-Gak sandstone deposits. 

Table 7A–5. Tabulation of reserves and resources of the Haji-Gak iron deposit. 

[Tabulation of data from Soviet exploration in the 1960s. NA, not available; wt. %, weight percent]

Soviet Equivalent Ore Ore, in million Iron, in wt. Sulfur, in 

category classification type metric tons % wt. %

A Measured or proven Oxidized ore 9.1 62.52 0.14

B Measured or proven Oxidized ore 19.2 62.69 0.09

C1 Indicated or probable Oxidized ore 65.1 62.15 0.13

C1 Indicated or probable Primary ore 16.2 61.3 4.56

C1 Indicated or probable Fragmental ore 1.2 60.62 0.08

C2 Inferred or possible All ore types 3,143 NA NA

C2 Inferred or possible Fragmental ore 2.9 NA NA

P2 Hypothetical resources All ore types 1,333.3 NA NA

P2 Hypothetical resources Fragmental ore 8.6 NA NA

Total 1,769.9
7A.11.1.1 Haji-Gak Barite Deposit

The Haji-Gak iron AOI contains five locations of barite mineralization. Barite ore occurs as 

veins 0.2 to 1.2 m thick and 15 or 25 to 135 m long in Proterozoic chlorite-sericite schist. In addition, 

barite debris has been found over an area of 10 km2

. The speculative reserves of the largest vein are 

36,200 metric tons (t) with an average barium oxide content of 56 percent. 

7A.11.1.2 Haji-Gak Limestone Deposit

The 64-m-thick Upper Devonian limestone extends for at least 800 to 900 m, for an area of 

45 km2, to a depth of 60 m, and contains 49.08 to 54.7 percent calcium oxide. The limestone can be 

used as flux raw material. The speculative reserves are 3.5 Mt. 

7A.11.1.3 Haji-Gak Sandstone Deposit

The deposit comprises Upper Devonian quartz sandstone that is 50 m thick and contains 93.66 to 

97.31percent percent silicon oxide. The speculative reserves are 650,000 t. A deposit of refractory rock 

represented by a lenticular body of quartzite-like sandstone and quartzite, 32 to 70 m thick, resting in 

Upper Devonian carbonate sequence, is located in the area of the Haji-Gak iron deposit. The quality of 

the raw material is suitable for manufacturing class-II dinas. 

7A.12 Northeastern and Farenjal Haji-Gak Subareas 

Several prospects and anomalies are present in the Northeastern Haji-Gak and Farenjal subareas 

of the Haji-Gak iron AOI (figs. 7A–26 and 7A–27). To the northeast of the main Haji-Gak mine 

(Haji-Gak prospect) subarea, several additional mineral occurrences similar to Haji-Gak are present, 

such as Khaish, Zerak, Kharzar, Chui, Sausang, Kharkiz, Darre-i-Neelee, and Surkh-i-Parso 

(fig. 7A–27). The Northeastern Haji-Gak subarea contains the Kharzar, Khaish, Chuy, and Zerak 

sedimentary-rock hosted iron deposits that have been explored. The largest of these iron prospects 

adjacent to the Haji-Gak prospect subarea is the Khaish prospect in Bamyan Province, which is hosted 

in the same Proterozoic rocks as Haji-Gak. The Zerak iron occurrence in Baghlan Province lies within a 

fault zone, and three 90- to 450-m-long and 12- to 75-m-wide hematite magnetite zones have been 

discovered to date. Speculative resources are 20 Mt iron ore grading up to 62.5 wt. % iron. The Khaish, 

Zerak, Kharzar, Chui, and Sausang iron prospects are considered eastward continuations of the Haji-Gak 

deposit. The ore content, the deposition processes, the shape, and the host rocks of the ores in these 

prospects are similar to Haji-Gak. The total prospecting reserves in these extensions is 300 Mt (Kusov 

and others, 1965). 

Chapter 7A. Summary of the Haji-Gak Iron Area of Interest 487

Table 7A–6. Location reserves and ore types of eastern prospects in the Northeastern Haji-Gak subarea.

[British Geologic Survey, NA, not available; wt. %, weight percent]

Reserves, in million Iron, in Name Longitude Latitude Ore type metric tons wt. %

Khaish 34°43′55′′N 68°12′30′′E 117 hematite and magnetite 55.54 1 Kharzar 34°41′46′′N 68°09′12′′E ~10 hematite, magnetite, and martite 62.76

Chuy 34°45′37′′N 68°13′00′′E NA hematite and magnetite 56.93

Zerak 34°46′36′′N 68°15′12′′E 20 hematite and magnetite 56.93

Sausang 34°45′08′′N 68°15′45′′E 300 hematite and magnetite NA

1

Assuming more than 100 meters along the strike
488 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

Figure 7A–25. Google Earth image with superimposed Haji-Gak iron orebodies. (a) Tilted image showing different 

types of orebodies. (b

These occurrences are described by Brueckl (1935, 1936), Momji and Chaikin (1960), and 

Bybochkin and Kurotchenko (1961). The iron occurrences are considered to be eastern extensions of the 

Haji-Gak iron deposit because they have similar host rocks, such as those in the Awband and Green 

Schist Formations. 

) Areal view showing orebodies and their designations. 
Chapter 7A. Summary of the Haji-Gak Iron Area of Interest 489

7A.12.1 Khaish Iron Prospect

The Khaish iron prospect is located at longitude 34°43'55" N. and latitude 68°12'30" E., on the 

upper reaches of the Khaish River (left tributary of Turkman River), on the south slope of a small ridge 

4.5 km to the southwest of Khaish village (fig. 7A–28). The occurrence is 8 km to the south from the 

road (Khaish-Chorde-Gorband). At the Khaish prospect, five prospects smaller than Khaish have been 

delineated to date that are 300- to 1,300-m-long and 10- to 20-m-thick and can be traced downdip for 

200 m. Speculative resource estimates at Khaish suggest that the deposit may contain up to 117 Mt, but 

at the low grades of 48.6 wt. % iron, 0.1 wt. % titanium, and 0.019 wt. % cobalt. 

The Khaish prospect contains five orebodies comprising blocky fragments of hematite-magnetite 

ore hosted in the Awband Formation. The orebodies are hosted in different lithologies and along 

different contacts. Orebody 1 lies along a contact with dolomitic limestone, orebodies 2 and 5 are hosted 

in sericite and quartz-sericite schist, orebody 3 is hosted along a contact with carbonate-chlorite schist; 

and orebody 4 is hosted along a contact between quartz-sericite schist and carbonate-chlorite-sericite. 

The contacts between the orebodies and the schist are sharp and planar, but contacts with dolomitic 

limestone are more diffuse and gradational (Kusov and others, 1965b).

Orebodies are lenticular, and at places, they conformably overlay host rocks (orebodies 2, 4, 5) 

or cut through the host rocks (orebodies 3, 4). The length of the orebodies varies from 300 to 1,300 m 

along the strike and as much as 200 m downdip (erosion), and the width varies from 10 to 200 m. 

Orebody 1 extends 300 m along the strike and 200 m downdip (stripped by erosion)is 200 m thick from 

surface to the middle part, and it is pinching out to the flanks. The azimuth of the dip of the orebodies is 

95° (orebody 3) and 160° to 175° (orebodies 1, 2, 4, and 5), and the angle of dip is 60° to 70°. The 

orebodies form a ridge as much as 15 to 20 m high. Fragmental ores are located to the south from 

natural ores (Kusov and others, 1965b).

The orebodies consist of massive and massive-banded oxidized hematite-magnetite ores with 

medium- and fine-grained texture and include pores. The rocks contain relicts of pyrite, which indicate 

the presence of sulfides in nonoxidized ore at the depth. The mineral content of the ore is listed in 

table 7A–6. 

Ores in the Khaish iron prospect are highly oxidized, and contain anomalous concentrations of 

cobalt and iron. The total length of the orebodies is 2,925 m, the average thickness is 50 m thick, the 

depth along the dip is 200 m, the volumetric weight is 4.0, and the amount of inferred (prospective ore) 

resource is 117 Mt (Kusov and others, 1965b).

Table 7A–6. Mineral content of the ore from the Khaish iron prospect. [Data are from Kusov and others (1965b). Al2O3, aluminum oxide; BaO, barium oxide; CaO, calcium oxide; Co, cobalt; Fe, 

iron; FeO and Fe2O3 , iron oxide; MgO, magnesium oxide; MnO, manganese oxide; P2O5, phosphorus pentoxide; S, sulfur; 

SiO2, silicon oxide; TiO2, titanium oxide; wt. %, weight percent] 

Mineral Content, in wt. %

Fe 48.12–62.97

Fe2O3 56.23–77.79

FeO 1.42–12.34

SiO2 4.00–7.28

Al2O3 0.20–1.24

TiO2 0.023–0.11

CaO 0.22–0.57

MgO 0.045–0.43

MnO 0.057–1.38

BaO 0.0–1.53

Co 0.07–0.019

P2O5 0.0–0.28

S 0.03–2.92

Lost in tempering 1.29–7.45
490 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

Figure 7A–26. Advanced Spaceborne Thermal Emission and Reflection (ASTER) radiometer image of the Northeastern Haji-Gak subarea showing known 

iron occurrences and prospects in relation to ASTER mineral anomalous zones. Data from Peters and others (2007).
Chapter 7A. Summary of the Haji-Gak Iron Area of Interest 491

Figure 7A–27. Advanced Spaceborne Thermal Emission and Reflection (ASTER) radiometer image showing the Farenjal barite subarea, which contains the 

Farenjal barite district in the north and the Surkh-i-Parso copper and uranium occurrence in the south. Data from Peters and others (2007)
492 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

Figure 7A–28.

7A.12.2 Kharzar Iron Prospect

The Kharzar iron prospect is located at longitude 34°41ʹ 46" N. and latitude 68°09'12" E., along 

the upper reaches of the Kharzar River, 1.2 km to the south from the Surhan path (fig. 7A–29). Kharzar 

iron occurrence lies in Proterozoic greenschist rocks and contains 70-m-wide and about 300-m-long 

hematite lenses grading up to 62.97 wt. % iron. The ore is hosted in the Green Schist Formation and 

comprises exposed natural ores and fragmental hematite-magnetite ores. The orebodies form lenticular 

shapes, which are 315 m long along the strike, 70 m wide, and pinch out along the flanks. The 

fragmental orebodies are located near the natural ores. The orebodies are hosted in quartz-sericitechlorite schist of the Green Schist Formation with different contacts; the ore and footwall contact with 

the host rocks is conformable, but the hanging wall contact is cross cutting. The azimuth of the orebody 

is 170°, and the dip angle is 70° (Kusov and others, 1965b).

The orebody comprises massive or massive-banded hematite-magnetite and martitized ores with 

fine-grained texture. Secondary pores appear within massive texture. Pyrite relicts are preserved. The 

mineral content of the ore is listed in table 7A–7. 

Map of the Khaish deposit, modified from a 1:25,000 map from Kusov and others (1965b).

Table 7A–7. Mineral content of the ore from the Kharzar iron prospect. [Data are from Kusov and others (1965b). Al2O3, aluminum oxide; BaO, barium oxide; CaO, calcium oxide; Co, cobalt; Fe, 

iron; FeO and Fe2O3, iron oxide; MgO, magnesium oxide; MnO, manganese oxide; P2O5, phosphorus pentoxide; S, sulfur; 

SiO2, silicon oxide; TiO2, titanium oxide; wt. %, weight percent]

Mineral Content, in wt. %

Fe 62.55–62.97

Fe2O3 70.73–72.61

FeO 15.25–17.71

SiO2 7.42–10.68

Al2O3 as much as 0.37

TiO2 0.032–0.043

S 0.011–0.11

MgO 0.045–0.23

CaO 0.17–0.25

MnO 0.042–0.076

BaO 0.02–0.032

Co 0.08–0.015

P2O5 0.074–0.4

Lost in tempering 0.85–1.71
7A.12.3 Chuy Iron Prospect

The iron-bearing Chuy prospect is located at longitude 34°45'37" N. and latitude 68°13'00" E., in 

the upper Chuy River. The Chuy iron prospect is 400 m long and 2.5 to 10 m wide and comprises a 

hematite-magnetite stratabound body within quartz-chlorite schist. The distance from the deposit to the 

road is 10 km. The ore deposit consists of one orebody, which comprises exposed and oxidized natural 

hematite-magnetite ore. The orebody is conformable with quartz-chlorite schist of the Awband 

Formation, the azimuth of dip is 190°, and the angle is 70°. The host rock for the orebody is the 

quartz-sericite schist. The content and structure of the ore is similar to Kharzar ore deposits. The ore 

content varies from 48.12 to 65.74 wt. % iron (Kusov and others, 1965b).

7A.12.4 Zerak Iron Prospect

The Zerak iron prospect is located at longitude 34°46'36" N. and latitude 68°15'12" E., in the 

upper reaches of the Burchistah River (left tributary of Turkman River) on the southern part of Koh-eBaba Ridge in Baghlan Province. The Zerak iron prospect lies within a fault zone, and three 90- to 

450-m-long and 12- to 75-m-wide hematite magnetite zones have been discovered to date. Speculative 

resources are 20 Mt of iron ore grading as much as 62.5 wt. % iron. The deposit contains three 

orebodies, the western, central, and eastern orebodies, which are hosted in the Awband Formation. The 

orebodies are platy, 90 to 450 m long along the strike, and 12 to 75 m thick. The largest orebody is 

located in the eastern part of the deposit; it is 450 m long along the strike, 75 m wide, and 450 m 

stripped by erosion along the dip. The three orebodies extend to the northeast, dipping southeast (140° to 

160°); the dip angle is 75° to 80°.(Kusov and others, 1965b). 

The central and western orebodies were conformably deposited in dolomitic limestone, and the 

contact is wavy. The eastern orebody footwall comes into contact with schist (derived from tuff), and the 

hanging wall comes into contact with quartz dolomite. The contact of the eastern orebody with schist is 

sharp and cross-cutting; with quartz dolomites, it is gradual. The fragmental ore occupies an area of 

50 km2

 and is located near the natural ore. The natural ore and fragmental ore comprise 

hematite-magnetite oxidized ore with massive and medium-grained texture with pores. The small pores 

are dispersed, and constitute up to 15 percent of the volume. The pore shape is irregular, the surface is 

covered by ore ochre, and the pyrite relicts are preserved. The mineralogy of the Zerak ore deposit is 

similar to that of the Kharzar deposit. The prospective ore reserve of Zerak deposit is 20 Mt (Kusov and 

others, 1965b).

7A.12.5 Khakriz Iron Prospect

The Khakriz iron prospect is located 5 km to the east of Zerak, 2.5 km to the south of the 

Shagdar path, and is connected by the Turkman valley (6 km long), the Kabul-Gorband road (24 km

long), and by trails. The ore outcrops as hematite (probably martite). The size, depositional conditions, 

and other aspects of the ore deposit are unknown (Manucharyants and others, 1963). 

7A.12.6 Sausang Iron Prospect

The Sausang iron prospect is located at latitude 34°45'08" N. and latitude 68°15'45" E., 2.2 km to 

the south of the Zerak iron prospect on the right slope of Burchistah River, to the west of the Sausang 

path (Abdullah and others, 1977). The prospect contains one small lenticular orebody, which outcrops 

along the top of the mountain and lies conformably in or on quartz-chlorite-sericite schist (derived from 

tuff and volcanic rocks). The contact of the ore with the schist is sharp and straight. The schist has been 

altered by seritization and silicification. The orebody outcrop is 350 m long and 15 m thick, the dip 

azimuth is 160°, and the angle is 60°. The orebody comprises hematite-magnetite ores similar to ores of 

the Zerak deposit. 

Chapter 7A. Summary of the Haji-Gak Iron Area of Interest 493
494 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

7A.12.7 Darre-i-Neel Iron Prospect

The Darre-i-Neel prospect is located at longitude 34°54' N. and latitude 68°34' E., in the upper 

reach of the Darre-i-Neelee stream, 9 km northeast of the Khakriz deposit. The ore comprises individual 

exposed ores and blocky martite float, which formed in skarns. The size, content, and depositional 

conditions of this ore deposit are unknown (Manucharyants and others, 1963; Kusov and others, 

1965a,b; Chmyriov and others, 1973). 

Figure 7A–29.

7A.12.8 Surkh-o-Parso Iron Prospect

Surkh-o-Parso is located at longitude 34°51' N. and latitude 68°39' E. near the mouth of the 

Turkman River, 30 km to the east from Darre-i-Neel. The region is connected with Gorband City by a 

winding path (11 km long). Blocky fragments of hematite-magnetite ore constitute the ore deposit; the 

size and depositional conditions are unknown. The Surkh-o-Parso prospect and ore manifestations are 

related to the same structure and suite of metamorphic rocks. Besides iron ores, lead-zinc-barite ores 

also are present in this area (Manucharyants and others, 1963). Disseminated chalcopyrite has been 

found over an area of 9 km2 in marmorized limestone and quartzite of Carboniferous to Early Permian 

age. Uranium minerals also have been found at the occurrence (Khananov and others, 1967). 

7A.12.9 Farenjal Barite Subarea

The Farenjal barite subarea contains barite deposits and occurrences in Paleozoic rocks and the 

Surkh-o-Parso iron-copper-uranium prospect (fig. 7A–30) (Abdullah and others, 1977). The Farenjal 

barite and lead-zinc ore district lies along the Gorband River basin, in an area underlain by Paleozoic 

carbonate-shale and volcanic rocks. The area is known for barite, lead, and zinc mineralization. The 

subordinate mineralization is represented by manganese, iron, copper, talc, and asbestos. The deposits 

and occurrences of the barite and lead-zinc ore formation are usually found in shear zones within Lower 

Carboniferous terrigenous-carbonate rocks feathering the Har-i-Rod Fault. The tops of the carbonate 

Schematic plan showing the Kharzar deposit, modified from a 1:5,000 schematic from Kusov and 

others (1965b).
Chapter 7A. Summary of the Haji-Gak Iron Area of Interest 495

barite veins are almost devoid of lead and zinc sulfides. From a depth of 100 m downdip, the calcitebarite ore grades into calcite-sulfide ore that is poor in barite and rich in lead and zinc. Stream sediment 

sampling revealed rich haloes of gold and cinnabar with scheelite, wolframite, and cassiterite. The 

source of these minerals is unknown. 

Figure 7A–30. Photographs of the Surkh-o-Parso copper-uranium prospect in the Haji-Gak iron area of interest. 

(a) North view of the Phanerozoic sequence at Surkh-o-Parso showing the northward dip of the sedimentary strata. 

(b) Photograph of whispy discontinuous quartz-pyrite veins in a 2-meter-wide zone. Photographs are by Robert 

Bohannon, U.S. Geological Survey.
496 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

7A.13 Summary of Potential

The Haji-Gak iron AOI contains the Haji-Gak iron deposit, a world class-size deposit, and 

several other iron prospects. Three subareas have been delineated within the main AOI that have 

additional potential for economic deposits. The Haji-Gak iron deposit is more than 32 km long and 

contains 16 separate zones, some of which are up 15 km long, 380 m wide, and extend 550 m downdip. 

Seven of these zones have been studied in detail. Previous Russian resource estimates for the entire 

deposit are 1,700 Mt. The Kharzar, Khaish, Chuy, Khakriz, and Zerak sedimentary-rock-hosted iron 

deposits are adjacent to and to the east of the main Haji-Gak iron deposit in the Northeastern Haji-Gak 

subarea and have also been explored. The Haji-Gak iron AOI also contains barite deposits and 

mineralization near the Haji-Gak prospect subarea and in the Farenjal subarea in the northeast of the 

AOI. The subordinate mineralization is represented by manganese, iron, copper, talc, and asbestos. 

Additionally, the Haji-Gak prospect subarea contains the Haji-Gak limestone deposit, which contains 

3.5 Mt of speculative resources in an area of 45 km

2

7A.14 Selected References

to a depth of 60 m. The Haji-Gak sandstone

deposit, also in the Haji-Gak prospect subarea, contains 650,000 t of speculative resources with a silicon 

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