Chapter 2C. Geohydrologic Summary of the Aynak Copper, 

Cobalt, and Chromium Area of Interest

By Thomas J. Mack and Michael P. Chornack

2C.1 Introduction

This chapter describes the geohydrology of the Aynak copper, cobalt, and chromium area of 

interest (AOI) in Afghanistan identified by Peters and others (2007). The AOI is located in southern 

Kabul, northern Logar, and eastern Wardak Provinces (fig. 2C–1a,b) and is part of the Kabul Basin. The 

Logar Valley subarea, at 1,013 km2 (square kilometers), is the largest subarea in the 3,439-km2 AOI.

Water is needed not only to process mineral resources in Afghanistan, but also to supply existing 

communities and the associated community growth that may accompany a developing mining economy. 

Information on the climate, vegetation, topography, and demographics of the AOI is summarized to 

provide information on the seasonal availability of, and seasonal demands for, water. The geohydrology 

of the AOI is described through the use of maps of streams and irrigated areas, generalized 

geohydrology and topography, and well locations. Where these data are available, the depth to water and 

height of static water in wells are documented. The results of lineament analyses are presented to 

identify areas where the rock may be more fractured than in other areas, which may be an indicator of 

high relative water yield and storage in bedrock aquifers. 

Afghanistan’s recent turbulent history has left many of the traditional archival institutions in 

ruins, and most water-resource and meteorological data-collection activities had stopped by 1980. 

Recently (2011), nongovernmental organizations (NGOs), foreign government agencies, and the Afghan 

government have begun water-resource investigations; however, these activities and the amount of data 

collected are limited. This report summarizes the satellite imagery and climatic, topographic, geologic, 

surface-water, and groundwater data available. Geohydrologic inferences are made on the basis of an 

integrated analysis of these data and an understanding of conditions in other areas of Afghanistan. 

2C.1.1 Climate and Vegetation

Climate information for the Aynak copper, cobalt, and chromium AOI is based on data generated 

for the Afghanistan agricultural-meteorological (Agromet) project. Agromet was initiated by the 

U.S. Agency for International Development and the United Nations Food and Agriculture Organization 

in 2003 to establish data-collection stations and develop country-wide agrometeorological services. 

Scientists with the Agromet project are assisting the Afghan Government to collect and analyze 

agricultural and meteorological data as they relate to crop production, irrigation, water supply, energy, 

and aviation. The U.S. Geological Survey (USGS) assumed responsibility for the operation of the 

project in 2005; by the end of August 2010, 87 Agromet stations were recording precipitation data and 

other parameters. Additionally, the Agromet project receives data from 18 Afghanistan Meteorological 

Authority (AMA) weather stations. The Agromet project has developed a database that includes data 

collected at the Agromet stations over the past 6 years (2005–2011), data collected at the AMA weather 

stations, and historical data collected at weather stations from 1942 to 1993. Data collected as part of the 

Agromet project are compiled annually by water year (September through August) and are reported in 

the Afghanistan Agrometeorological Seasonal Bulletin (Seasonal Bulletin) published by the Ministry of 

Agriculture, Irrigation, and Livestock. Unless otherwise specified, the Agromet data cited in this report 

are from the agricultural season that extends from 1 September, 2009, to 31 August, 2010. 
136 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

a 
Chapter 2C. Geohydrologic Summary of the Aynak Copper, Cobalt, and Chromium Area of Interest 137

b 

Figure 2C–1. (a) Landsat image showing the location of, and (b) place names, stream names, and 

streamgage station numbers in, the Aynak copper, cobalt, and chromium area of interest in southeastern 

Afghanistan.
138 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

The AOI is located in the Capital region of the Agromet network and includes several 

precipitation stations (Ministry of Agriculture, Irrigation, and Livestock, 2010). The yearly observed 

total precipitation for the AOI in the 2009–2010 water year as reported in the Seasonal Bulletin 

(Ministry of Agriculture, Irrigation, and Livestock, 2010, map 2) ranged from 221 to 300 mm 

(millimeters). Available data for the Kabul Agromet station, just inside the northern border of the AOI in 

Kabul, include 2009–2010 water year and long-term average (LTA) precipitation and temperature data.

An Agromet station located in the southeast corner of the Logar Valley subarea had a total of 7 

snow days during the 2009–2010 water year, distributed as follows: November and December 2009, 1 

snow day each; January 2010, 2 snow days; and February 2010, 3 snow days. During the 2009–2010 

water year, this station received a total of 48 cm (centimeters) of snow, compared to the LTA of 137 cm. 

The Afghanistan snow-depth map in the 2009–2010 Seasonal Bulletin (Ministry of Agriculture, 

Irrigation, and Livestock, 2010) showed that the AOI had 2 to 10 cm of snow cover on 17 January, 

2010, but this snow cover was estimated prior to the 3 days of snow in February 2010. 

A statistical summary of precipitation and temperature data for the Kabul Agromet station is shown in 

table 2C–1. 

The “Potential Natural Vegetation” described in Breckle (2007) is the vegetation cover that 

would be present if not modified by human activity. Today, as a result of continued exploitation such as 

grazing, farming, and deforestation, much of the original natural vegetation is found only in a few 

remote areas of Afghanistan. The destruction of the natural vegetation has resulted in the degradation 

and erosion of the soil cover in some areas. Many areas exhibit signs of long-lasting desertification 

caused by human activity.

Although the natural vegetation in Afghanistan has been severely degraded, there are some areas 

where native vegetation is still dominant, such as high and remote mountain regions and extreme desert 

environments. The “Map of potential natural vegetation” in Breckle (2007, fig. 2) shows two vegetation 

zones within the AOI. The vegetation zones are controlled by elevation, climate, and amount of soil 

development. Much of the surface of the AOI above the basin bottoms is bedrock outcrop and has very 

sparse vegetation. The lower elevations are classified as Pistacia atlantica woodlands, which give way 

to Amygdalus woodlands (Breckle, 2007); however, there is very little actual woodland. Irrigated fields 

and pastures are present in the valleys in the AOI wherever water can be accessed, and small orchards 

may be present (fig. 2C–3).

Table 2C–1. Annual, long-term annual average, and long-term average minimum and maximum precipitation and 

temperature at the Kabul Agrometeorological (Agromet) station in the Aynak copper, cobalt, and chromium area of 

interest in southeastern Afghanistan. ° [AOI, area of interest; km, kilometers; m, meters; mm, millimeters; C, degrees Celsius]

Precipitation Temperature

Distance Long-term average1 Long-term average1 2009- Agromet from AOI Elevation Maximum 2010 Monthly station center (m) Annual Monthly maximum Minimum and Monthly and annual minimum and (km) (mm) and month (mm) month (°C) mean (°C) month (mm) month (mm) (°C)

Kabul 24 1,810 304.3 317.5 1.2 June and 83.2 April –2.6 January 9.8 24.8 July

August

1

Long-term averages are based on data from 1942 to 1993 and 2005 to 2010 as reported in the Afghanistan 

Agrometeorological Seasonal Bulletin (Ministry of Agriculture, Irrigation, and Livestock, 2010).
Chapter 2C. Geohydrologic Summary of the Aynak Copper, Cobalt, and Chromium Area of Interest 139

Figure 2C–2. Historical streamgage locations, digitally generated drainage network, and irrigated areas in the 

Aynak copper, cobalt, and chromium area of interest in southeastern Afghanistan.
140 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

Figure 2C–3. Photograph showing the Chakari River basin looking south from the Kharuti Dawrankhel subarea, 

Aynak copper, cobalt, and chromium area of interest in southeastern Afghanistan.

2C.1.2 Demographics

Population density in Kabul ranges from greater than 5,000/km2 within the metropolitan area to 

2,501 to 5,000/km2 in the surrounding urban areas of the Aynak copper, cobalt, and chromium AOI as 

mapped by LandScan (Oak Ridge National Laboratory, 2010). Kabul, the capital of Afghanistan, is 

located at the northern boundary of the AOI (fig. 2C–1b). Some small areas in the northern part of the 

AOI near the junction of the Kabul and Paghman Rivers have densities greater than 20,000/km2

. Dense 

populations in the AOI are concentrated along the Kabul and Logar Rivers; these populated areas 

coincide with irrigated areas (fig. 2C–2). The city of Kabul has a population greater than 4 million and 

the greatest population density in Afghanistan. The population density shown in figure 2C–4 has a pixel 

resolution of about 1 km2

 (Oak Ridge National Laboratory, 2010). 

Elsewhere in the AOI are many small settlements with population densities in the range of 101 to 

500/km2 (fig. 2C–4). The population density away from the rivers, in the basins without perennial 

streams, and in the upland areas ranges from 0 to 50/km2. For example, the areas of the Chakari River 

basin south of the Bakhel Charwaz and Kharuti Dawrankhel subareas are largely uninhabited (fig. 2C–

3). Much of the smaller subareas in the AOI, particularly the Yagh-Darr Gull Darra and Bakhel Charwaz 

(fig. 2C–1b), are generally populated only where springs flow from upland areas. The high, rugged 

mountains in the AOI are uninhabited (fig. 2C–3). Afghanistan Highway 1 is a primary road in the 

western part of the AOI, and Afghanistan Highway 76 (not shown) follows the Logar River through the 

AOI (fig. 2C–1b). With the exception of Highways 1 and 76, and the roads and streets within the capital 

city of Kabul, all roads in the AOI are mapped as “tracks” on the district maps for this area (Afghanistan 

Information Management Service, 2004). 
Chapter 2C. Geohydrologic Summary of the Aynak Copper, Cobalt, and Chromium Area of Interest 141

Figure 2C–4. Population density of the Aynak copper, cobalt, and chromium area of interest in southeastern 

Afghanistan.
142 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

2C.1.3 Topography and Geomorphology

The topography of the Aynak copper, cobalt, and chromium AOI is dominated by the river 

valleys formed by the Kabul, Logar, and Chakari Rivers (fig. 2C–1a,b

The geomorphology of the AOI is dominated by the Kabul, Logan, and Chakari Rivers, and the 

northeast-trending structural fabric (fig. 2C–5) (Bohannon and Turner, 2005). The mountainous areas on 

the western and eastern borders of the AOI are dissected by streams that form dendritic drainage 

patterns, although structure appears to control some of the drainage patterns (fig. 2C–2).

). The middle of the AOI is a wide 

valley formed by the drainage network of the Logar River. The elevation of the valley ranges from 1,800 

m (meters) above sea level (asl) along the Logar River to 2,000 m asl. The valley is flanked on the east 

and west by high mountains that generally trend north-northeast. The mountains in the western half of 

the AOI have many peaks whose elevations exceed 4,000 m asl. In the lower reaches of many of the 

smaller streams, the relief between the stream bottoms and flanking ridge tops is 1,000 m. The 

mountains in the eastern part of the AOI also have some peaks whose elevations exceed 4,000 m asl; 

most high peaks have elevations of about 3,500 m asl. In these mountains, relief between valley bottoms 

and ridge tops commonly exceeds 1,000 m (Bohannon, 2005). A prominent topographic feature in the 

western part of the AOI is a long, north-northeast-trending fault-controlled valley (fig. 2C–5) (Bohannon 

and Turner, 2005; Davis, 2006). 

2C.2 Geohydrology

The geohydrology of Afghanistan has been described in general terms by Abdullah and 

Chmyriov (1977, book 2). As defined in their “Geology and mineral resources of Afghanistan,” the 

Aynak copper, cobalt, and chromium AOI is in the “Central Afghanistan Hydrogeological Folded 

Region that occupies the central part of the country with a predominantly mountain climate.” The 

outcrops and near-surface rocks in the AOI can be grouped according to their physical and hydraulic 

properties. The generalized geohydrology of the AOI is shown in figure 2C–5 with the underlying 

topography to allow examination of the geohydrology in the context of relief. Figure 2C–6a shows the 

generalized geohydrology without topography for a clearer depiction of the geohydrologic units. Wells 

present in the map area (discussed in the Groundwater section) are shown in figures 2C–6a and b. 

Generalized geohydrologic groups were created from a country-wide geologic coverage (Doebrich and 

Wahl, 2006) by combining sediments and rocks into major sediment- or rock-type groups of similar 

hydrologic characteristics. The geohydrologic groups in and near the AOI, ranked from high to low 

relative hydraulic conductivity (Freeze and Cherry, 1979, table 2.3), are “river channel; sands, 

undifferentiated; loess and fine sediments; conglomerate sediments and rocks; limestones and 

dolostones; sedimentary rocks; metamorphic rocks; and intrusive rocks and lavas” (figs. 2C–5, 2C–6a

The conglomerate sediments and rocks geohydrologic group is mapped primarily as scattered 

outcrops in upland basins (fig. 2C–5); however, this group underlies most surficial sediment in the basin 

bottoms and has been described as semi-consolidated (Böckh, 1971; Mack and others, 2010). The 

surface area of some of these outcrops is large (as much as 60 km

). 

Doebrich and Wahl (2006) used geologic maps at a scale of 1:250,000, modified from Russian and 

Afghan Geological Survey (AGS) mapping, to generate the country-wide geologic coverage. The 

1:250,000-scale geologic map that cover this AOI is provided by Bohannon and Turner (2005). 

2

). The measured thickness of basin 

deposits in the AOI is at least 600 m in some places (Japan International Cooperation Agency, 2007), 

and their estimated thickness is as much as 1,000 m in some areas of the AOI (Homilius, 1969).
Chapter 2C. Geohydrologic Summary of the Aynak Copper, Cobalt, and Chromium Area of Interest 143

Figure 2C–5. Topography and generalized geohydrology in the Aynak copper, cobalt, and chromium area of 

interest in southeastern Afghanistan.
144 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

a 
Chapter 2C. Geohydrologic Summary of the Aynak Copper, Cobalt, and Chromium Area of Interest 145

b 

Figure 2C–6. (a) Generalized geohydrology, mapped faults, well locations, and depth to water, and (b) 

geohydrology and height of static water in well casings in community supply wells in the Aynak copper, cobalt, and 

chromium area of interest in southeastern Afghanistan.

The consolidated rocks in the AOI are grouped by rock type (including chemistry and genesis) 

and include sedimentary rocks; limestones and dolostones; metamorphic rocks; and intrusive rocks and 

lavas. This grouping also reflects the type and amount of porosity in these geohydrologic groups. The 
146 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

sedimentary rocks group (detrital sedimentary rocks such as sandstone and siltstone) and the limestones 

and dolostones group both have interstitial porosity. Both these groups can also have secondary fracture 

porosity, and in limestone the presence of solution cavities can greatly increase the secondary porosity. 

Outcrops of these two geohydrologic groups are limited in the AOI, but the limestones and dolostones 

group is present in the eastern part. The Yagh-Darra Gul-Darra subarea and the Bakhel Charwaz subarea 

(fig. 2C–1b) have extensive outcrops of the limestones and dolostones geohydrologic group (fig. 2C–5).

Very few, if any, wells are shown in this geohydrologic group (figs. 2C–6a and b

Rocks in the intrusive rocks and lavas group generally have minimal matrix (interstitial) 

porosity. The porosity in this group is a result of secondary fracturing from either cooling or tectonic 

activity. In the absence of seismo-tectonic fractures, the porosity of intrusive rocks such as granites is 

low to near zero. The presence of faults, fault zones, and fracture zones can increase the porosity of 

intrusive rocks and lavas. The metamorphic rocks have low matrix porosity but, depending on the 

degree of metamorphism, interstitial voids could remain in the rock. The movement of fluids through 

connected pore space in metamorphic rocks could be preferentially oriented parallel to bedding. The 

fracture porosity in metamorphic rocks can result from compaction foliation and be preferentially 

oriented along bedding. Secondary fracture porosity in metamorphic rocks can also be the result of 

tectonic activity. The porosity of this unit could be enhanced near faults, fault zones, and fracture zones. 

The intrusive rocks are present in the Logar Valley subarea and the southeast corner of the AOI. Very 

few wells are installed in this geohydrologic unit (fig. 2C–6

). The absence of wells 

in this geohydrologic unit is likely the result of the lack of hard-rock drilling equipment and the 

prohibitive expense of such drilling. 

a), mostly likely because of the prohibitive 

expense of drilling. The headwaters of the Chakari River are located at the contact between the 

limestones and dolostones group and the intrusive rocks and lavas group in the southeast corner of the 

AOI (figs. 2C–5). 

2C.2.1 Surface Water

A network of major streams, mostly perennial streams, modified from AIMS (Afghanistan 

Information Management Services, 1997) and VMAP1 (National Imagery and Mapping Agency, 1995), 

in the Aynak copper, cobalt, and chromium AOI is shown in figure 2C–2. A network representing likely 

ephemeral streams, generated with a digital elevation model (DEM), also is shown in figure 2C–2. 

Names of major streams and identification numbers for any streamgages and ungaged streamflow 

estimation sites in the AOI are shown in figure 2C–1b. The Kabul and Logar Rivers transect the AOI 

and the Chakari River originates within the AOI (fig. 2C–1b). The headwaters of the Kabul and Logar 

Rivers are located in mountainous regions southwest of Kabul. Most precipitation falls as snow, and 

seasonal melting and runoff account for the peak streamflows in the AOI in April (Mack and others, 

2010). Historical streamflow data are available for the Kabul, Logar, and Chakari Rivers (Olson and 

Williams-Sether, 2010; Vining, 2010). A few small dams and reservoirs are present on some of the 

tributary streams in the AOI. The dams appear to be used to store water for irrigation, but may also be 

used for flood control. 

The Kabul River enters the AOI at its northwest corner and flows about 70 km to the city of 

Kabul, where it exits the AOI. Where the river crosses mountain ranges, the stream valley is incised and 

has steep sides. In other areas, the valley bottom is wide enough to accommodate irrigated agricultural 

fields (fig. 2C–2). Two historical streamgage stations are located on the Kabul River in the AOI 

(fig. 2C–1b). The streamgage station farthest upstream, Kabul River at Maidan (Afghan identification 

number 1-0.000-9M), is located where the Kabul River enters the Logar Valley subarea at its western 

border (Vining, 2010). This station is at an elevation of 2,130 m asl and has a drainage area of 1,305 km2

and a period of record that extends from 1 October, 1961, to 30 September, 1980 (Vining, 2010). The 

annual mean streamflow for the period of record is 5.09 m3/s (cubic meters per second), with a standard 

deviation of 2.31 m3

/s. The mean annual streamflow per unit area for this station is 0.004 m3/s/km2. The 

month with the highest annual mean streamflow is April, with 20.7 m3

/s, and the month with the lowest 
Chapter 2C. Geohydrologic Summary of the Aynak Copper, Cobalt, and Chromium Area of Interest 147

annual mean streamflow is September, with 0.92 m3/s. The highest maximum monthly mean streamflow 

was 50.3 m3/s for April 1980. The lowest minimum monthly mean streamflow was 0.206 m3

The other streamgage station on the Kabul River in the AOI is the Kabul River at Tangi Saidan 

(Afghan identification number 1-0.000-8M). This station is located just outside the northern border of 

the Logar Valley subarea (fig. 2C–1

/s for 

July1980. A statistical summary of monthly and annual mean streamflows for this station is presented in 

table 2C–2 (Vining, 2010). Statistical summaries of streamflow data for all available historical gages in 

Afghanistan can be accessed at http://afghanistan.cr.usgs.gov/water.php. 

b). This station is at an elevation of 1,875 m asl, has a drainage area 

of 1,625 km2, and has a period of record that extends from 1 October, 1961, to 30 September, 1980 

(Vining, 2010). The annual mean streamflow for the period of record is 4.05 m3/s, with a standard 

deviation of 2.09 m3/s. The mean annual streamflow per unit area for this station is 0.002 m3/s/km2. The 

month with the highest annual mean streamflow was April, with 17.2 m3/s, and the month with the 

lowest annual mean streamflow was September, with 0.31 m3

/s. The highest maximum monthly mean 

streamflow was 43.9 m3/s for April 1980. The lowest minimum monthly mean streamflow was 0.070 

m3

The Logar River flows from south to north for about 56 km through the AOI and drains into the 

Kabul River just north of the AOI (fig. 2C–1

/s for June, 1971. A statistical summary of monthly and annual mean streamflows for this station is 

presented in table 2C–3 (Vining, 2010). 

b). The streamgage station on the Logar River at Sang-iNaweshta (Afghan identification number 1-10.R00-1A) is located between the Logar Valley subarea and 

the Yagh-Darra Gul-Darra subarea (fig. 2C–1b). This station is at an elevation of 1,805 m asl, has a 

drainage area of 9,735 km2, and has a period of record that extends from 1 October, 1961, to 30 

September, 1980 (Vining, 2010). The annual mean streamflow for the period of record is 9.63 m3

/s, with 

a standard deviation of 2.81 m3/s. The mean annual streamflow per unit area for this station is 0.00098 

m3

/s/km2. The month with the highest annual mean streamflow was April, with 22.9 m3/s, and the month 

with the lowest annual mean streamflow was September, with 0.75 m3/s. The highest maximum monthly 

mean streamflow was 45.9 m3/s for April 1965. The lowest minimum monthly mean streamflow was 

0.006 m3

/s for June 1971. A statistical summary of monthly and annual mean streamflows for this 

station is presented in table 2C–4 (Vining, 2010). 

Table 2C–2. Statistical summary of monthly and annual mean streamflow for

streamgage station. 3 [m /s, cubic meters per second]

1-0.000-9M KABUL RIVER AT MAIDAN

the Kabul River at Maidan 

Maximum Minimum

Month Streamflow Water year of Streamflow Water year of Streamflow

(m3/s) occurrence (m3/s) occurrence (m3/s) 

Mean

Standard

deviation

3 (m /s)

Percentage Coefficient of of annual variation streamflow

October 2.46 1966 0.434 1980 1.08 0.55 0.51 1.77

November 3.40 1966 0.460 1972 1.63 0.91 0.56 2.67

December 3.78 1966 0.391 1972 2.12 1.00 0.47 3.46

January 4.16 1968 0.799 1972 2.50 0.96 0.38 4.10

February 4.25 1968 1.45 1972 2.65 0.77 0.29 4.33

March 12.4 1973 2.60 1963 6.65 3.27 0.49 10.9

April 50.3 1980 6.17 1970 20.7 12.8 0.62 33.8

May 31.8 1965 1.74 1971 14.4 9.73 0.68 23.5

June 20.6 1965 0.742 1971 5.71 5.42 0.95 9.34

July 6.99 1965 0.206 1980 1.72 1.49 0.87 2.81

August 2.75 1965 0.236 1980 1.09 0.53 0.49 1.79

September 1.81 1965 0.338 1980 0.92 0.35 0.38 1.50

Annual 9.10 1965 1.72 1971 5.09 2.31 0.45 100
148 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

Table 2C–3. Statistical summary of monthly and annual mean streamflow for the Kabul River at Tangi Saidan 

streamgage station. 3 [m /s, cubic meters per second]

1- 0.000-8M KABUL RIVER AT TANGI SAIDAN

Maximum Minimum Mean

Standard Percentage Month Streamflow Water year of Streamflow Water year of Streamflow Coefficient of deviation of annual (m3/s) occurrence (m3/s) occurrence (m3/s) variation 3 (m /s) streamflow

October 1.20 1966 0.128 1980 0.44 0.30 0.68 0.90

November 2.57 1966 0.219 1972 1.05 0.79 0.74 2.16

December 3.52 1966 0.417 1972 1.61 0.96 0.60 3.30

January 4.15 1962 0.961 1971 2.48 0.97 0.39 5.09

February 4.57 1968 1.31 1971 2.67 0.92 0.34 5.47

March 12.5 1968 1.56 1963 6.15 3.01 0.49 12.6

April 43.9 1980 3.48 1970 17.2 10.5 0.61 35.3

May 26.8 1965 0.406 1970 11.1 8.21 0.74 22.7

June 18.1 1965 0.070 1971 4.38 5.13 1.17 8.98

July 6.83 1965 0.079 1971 1.00 1.55 1.55 2.04

August 1.31 1965 0.076 1980 0.40 0.29 0.72 0.81

September 0.572 1962 0.097 1971 0.31 0.15 0.50 0.63

Annual 7.96 1965 1.13 1971 4.05 2.09 0.51 100

Table 2C–4. Statistical summary of monthly and annual mean streamflow for

streamgage station. 3 [m /s, cubic meters per second]

1- 10.R00-1A Logar River at Sang-i-Naweshta

the Logar River at Sang-i-Naweshta 

Maximum Minimum

Month Streamflow Water year of Streamflow Water year of Streamflow (m3/s) occurrence (m3/s) occurrence (m3/s)

Mean

Standard Percentage Coefficient of deviation of annual variation 3 (m /s) streamflow

October 11.2 1966 0.212 1975 3.82 3.43 0.90 3.29

November 20.3 1966 3.14 1972 10.9 4.65 0.43 9.38

December 20.3 1966 7.99 1972 14.4 3.18 0.22 12.4

January 20.1 1962, 1966 10.5 1972 15.8 2.85 0.18 13.6

February 20.1 1969 10.2 1972 15.8 2.77 0.18 13.6

March 27.1 1968 11.1 1979 17.4 3.97 0.23 15.0

April 45.9 1965 7.07 1963 22.9 12.6 0.55 19.7

May 39.0 1965 0.235 1971 10.3 11.1 1.08 8.87

June 9.44 1965 0.084 1970 1.58 2.36 1.49 1.37

July 9.16 1978 0.006 1971 1.55 2.57 1.66 1.34

August 3.87 1978 0.017 1971 0.80 1.12 1.40 0.69

September 3.68 1965 0.030 1975 0.75 0.95 1.27 0.64

Annual 15.8 1965 5.48 1971 9.63 2.81 0.29 100

The headwaters of the Chakari River are in the mountains in the southeast corner of the AOI, in 

an area mapped as the contact between the limestones and dolostones geohydrologic group and the 

intrusive rocks and lavas geohydrologic group (fig. 2C–5). The Chakari River flows north for about 

50 km and drains into the Kabul River north of the AOI (fig. 2C–1b). The streamgage station on the 

Chakari River at Band-i-Amir Ghazi (Afghan identification number 1-9.R00-4W) is located in the 

Kharuti Dawrankhel subarea (fig. 2C–1b). This station is at an elevation of 2,050 m asl, has a drainage 

area of 395 km2 that includes approximately 3 km2 of irrigated area, and has a period of record that 

extends from 26 May, 1965, to 30 September, 1980 (Olson and Williams-Sether, 2010). The annual 

mean streamflow for the period of record is 0.31 m3

/s, with a standard deviation of 0.12 m3/s. The mean 

annual streamflow per unit area for this station is 0.0008 m3

/s/km2. The month with the highest annual 

mean streamflow was May, with 0.55 m3

/s, and the month with the lowest annual mean streamflow was 

January, with 0.05 m3/s. The highest maximum monthly mean streamflow was 1.71 m3/s for April 1980. 

The lowest minimum monthly mean streamflow was 0.01m3/s for January 1997, February 1977, and 

March 1978. The Chakari River was observed to be dry during a field reconnaissance visit on 
Chapter 2C. Geohydrologic Summary of the Aynak Copper, Cobalt, and Chromium Area of Interest 149

21 November, 2009. A statistical summary of monthly and annual mean streamflows for this station is

presented in table 2C–5 (Olson and Williams-Sether, 2010). 

There are no mapped springs in the VMAP database (National Imagery and Mapping Agency, 

1995); however, springs and karezes are present in the region, and the quality of water in at least two of 

these features in the AOI has been measured (Mack and others, 2010). During a field reconnaissance 

visit on 21 November, 2009, a spring was observed originating from highly fractured gneiss on the north 

flank of the Yagh-Darra Gul-Darra subarea. The spring, which had a volumetrically measured flow of 

approximately 0.1 L/s (liters per second) near its source, was managed by villagers for irrigation. Where 

it was measured, at an elevation of about 2,100 m asl, the spring was less than 1 km from the 

topographic peak (2,600 m asl) in the Yagh-Darra Gul-Darra subarea. An ephemeral spring was 

identified on the flank of a south-facing gully in the Kelaghy-Kakhay subarea. The spring, at an 

elevation of about 2,400 m, was about 0.7 km below a 2,700-m-high peak consisting of fractured 

carbonate rocks. The spring was not flowing when it was identified during the August 2010 

reconnaissance trip; however, there were small orchards at its origin and a settlement downgradient 

along the spring channel. Both factors indicate a likely dependence on increased accessibility of 

groundwater resources, such as a shallow depth to groundwater, in the area of the spring. The springs 

identified in the Yagh-Darra Gul-Darra and Kelaghy-Kakhay subareas coincide with lineaments 

identified as part of this project (discussed in the Lineament Analyses section). 

Table 2C–5. Statistical summary of monthly and annual mean streamflows for the Chakari River at Band-i-Amir 

Ghazi streamgage station. 3 [m /s, cubic meters per second]

1-9.R00-4WCHAKARI RIVER AT BAND-I-AMIR GHAZI

Maximum Minimum Mean

Standard Percentage Month Streamflow Water year of Streamflow Water year of Streamflow Coefficient of deviation of annual (m3/s) occurrence (m3/s) occurrence (m3/s) variation 3 (m /s) streamflow

October 0.68 1968 0.05 1972 0.33 0.17 0.53 8.80

November 1.06 1968 0.10 1971 0.34 0.24 0.73 9.06

December 0.94 1968 0.02 1978 0.15 0.22 1.53 3.95

January 0.25 1967 0.01 1978 0.05 0.06 1.33 1.22

February 0.38 1967 0.01 1978 0.10 0.11 1.17 2.57

March 0.62 1980 0.01 1977 0.18 0.21 1.20 4.80

April 1.71 1980 0.03 1975 0.44 0.40 0.89 12.0

May 0.96 1967 0.05 1975 0.55 0.26 0.47 14.9

June 0.93 1974 0.04 1971 0.52 0.29 0.56 14.0

July 0.97 1980 0.03 1971 0.39 0.23 0.58 10.7

August 0.94 1980 0.05 1971 0.34 0.22 0.65 9.14

September 0.86 1979 0.06 1971 0.33 0.20 0.59 8.99

Annual 0.58 1980 0.11 1971 0.31 0.12 0.39 100

2C.2.2 Groundwater

Information about groundwater resources in the Aynak copper, cobalt, and chromium AOI is 

limited at this time to shallow-well data. Approximately 2,500 shallow community groundwater-supply 

wells installed by NGOs in the AOI are in a database maintained by the Danish Committee for Aid to 

Afghan Refugees (DACAAR, 2011). Well-depth and static-water-level information is available for most 

wells in this database (figs. 2C–6a,b). About 80 percent of the supply wells are less than 30 m deep and 

all are less than 100 m deep. The depth to water in the supply wells in the AOI is generally less than 

15 m (fig. 2C–6a). The median depth to water is 11 m and about half of the wells are 5 to less than 15 m 

deep. The depth to water generally increases with distance from streams or with proximity to the basin 

walls (fig. 2C–6a). Depth to water in many wells in highly populated areas, such as Kabul (fig. 2C–4), is 

30 m or more as a result of groundwater withdrawals. 
150 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

Little well-construction information is available; however, most wells are “tube” wells, driven 

wells with polyvinyl chloride (PVC) casing, or dug wells constructed with concrete ring casing. Wells 

are generally installed in unconsolidated sediments, and completed a few meters below the first water 

depth encountered, and equipped with a hand pump. Figure 2C–6b shows height of static water in the 

water-supply well casings (well depth minus static depth to water). The median height of static water in 

well casings is 4 m. Spatially, most wells contain less than 3 m of static water. Many of the wells with 

3 m of static water or less were drilled in the early 2000s or pre-2000, and some may currently be 

inoperable. Wells with little static water were found to be vulnerable to seasonal water-level fluctuations 

and becoming dry for extended periods of time, or even permanently, in areas of the Kabul Basin where 

groundwater withdrawals are increasing (Mack and others, 2010). 

The water-supply wells are concentrated along the Kabul and Logar Rivers, with some 

concentrations of wells in other alluvial valleys (fig. 2C–6a). The recharge to the alluvial aquifer(s) in 

the river valleys is probably derived from the infiltration of streamflow and leakage from irrigated areas.

There could also be a small component of recharge from local precipitation, particularly as snowmelt 

runoff from the mountainous areas. Some shallow wells are located in areas mapped as the conglomerate 

sediments and rocks geohydrologic unit (fig. 2C–6a). Most of these areas are upland areas with no 

perennial streams. The groundwater recharge in these areas would most likely be from local 

precipitation; however, Mack and others (2010) measured a component of recharge consisting of 

groundwater inflows, through sediment and rock, from the mountain range east of the AOI in a similar 

basin about 10 km north of the AOI. 

Eight groundwater-monitoring wells (GWMs 4, 8, 10, 12, 17, 105, 128, and 142) in the AOI are 

monitored by DACAAR for groundwater levels and specific conductance. Five of the wells are in the

AOI subareas (fig. 2C–6a). Hydrographs provided by DACAAR for wells in the AOI are presented in 

appendix 3. The hydrographs show the date in week number and year, groundwater specific conductance

in microsiemens per centimeter at 25°

 Celsius (μS/cm), and depth to water in meters below ground 

surface (bgs). Of the wells in the subareas, four are located immediately adjacent to stream channels and 

the fifth (GWM 17) appears to be on an alluvium-covered upland basin or side slope about 2 km west of 

the Logar River. All of the monitoring wells are likely constructed entirely in alluvial material.

GWM 8 is located in the Kabul River valley in the “river channel” geohydrologic unit in the 

northwest corner of the Logar Valley subarea (fig. 2C–6a). River-channel sediments in the Kabul River 

Basin have been found to have a hydraulic conductivity of several hundred meters per day (Böckh, 

1971). The well depth of GWM 8 is reported to be 10 m bgs. The water-level hydrograph for this is 

fairly flat at slightly less than 10 m bgs across the period of record, with three sharp peaks that occur in 

late April and early May during 2007, 2008, and 2009. The first and last peaks show about the same 

water-level rise to 7.5 m bgs and the second peak shows a water-level rise to 9 m bgs. Specific 

conductance increases along with the water-level peaks. GWM 8 is located about 1 km from the Kabul 

River at Maidan streamgage station. There are no streamflow records for this station that coincide with 

the water-level period of record in GWM 8, but the LTA for the Kabul River at Maidan streamgage 

station indicates that the maximum streamflow occurs during April and May. It appears that recharge 

from the Kabul River is supplying water to the shallow alluvial aquifer in the Kabul River valley. 

GWM 10 is located in the valley of an ephemeral stream (in the “river channel” geohydrologic 

group) that is a tributary to the Kabul River (fig. 2C–6a). The total depth of the well is 42 m bgs. The 

period of record for the hydrograph is from week 19, 2005, through week 3, 2011. The water-level 

hydrograph shows distinct peaks (high water levels) that probably represent times when water was 

flowing in the ephemeral stream and valleys. Low water levels likely represent times of no flow in the 

ephemeral stream. The peaks are generally in the late spring and early to mid-summer; the lows are in 

early winter. The maximum water level during the period of record was about 16 m bgs during 

week 25, 2007. This area and much of Afghanistan experienced a drought that lasted from about 1999 to 

the mid-2000s (Akbari and others, 2007; Mack and others, 2010); however, the minimum water level 

(24 m bgs) appears to be the last measurement made during the period of record (late 2010). Maximum 
Chapter 2C. Geohydrologic Summary of the Aynak Copper, Cobalt, and Chromium Area of Interest 151

and minimum water levels in this well generally declined during the period of record. The 

specific-conductance hydrograph for the period of record fluctuates, but generally mirrors the 

water-level hydrograph–that is, high specific conductance is correlated with high water levels.

Three GWMs—17, 128, and 142—are located in the Logar River valley (fig. 2C–6a), in the 

“loess and fine sediments” geohydrologic unit. GWMs 128 and 142 are adjacent to the active stream 

channel, whereas GWM 17 is 2 km from the valley bottom and is located on an alluvial deposit that is 

adjacent to outcrops of the intrusive rocks and lavas geohydrologic group (fig. 2C–6a

GWM 142 is 53 m bgs with a period of record that extends from week 24, 2007, until 

week 36, 2010. The water-level hydrograph for this well is flat (at 12.6 m bgs) from the start of the 

period of record until week 12, 2008, when it rises sharply (to 12.3 m bgs) and then declines. The water 

level then gradually increases to about 12.4 m bgs at about week 52, 2008. The remainder of the period 

of record displays the typical seasonal highs and lows associated with streamflow. The specificconductance record for this well begins at about week 12, 2009, but shows a distinct peak in specific 

conductance during the winter months of 2009–2010. The water levels in this well are probably related 

to the flow in the Logar River. 

). GWM 128 is 

13.5 m bgs. The period of record extends from week 18, 2007, until week 37, 2010. The water-level 

hydrograph exhibits distinct highs and lows. The highs generally occur in the spring and summer 

months, and the lows occur in late summer through winter. The water level in this well probably reflects 

the flow in the Logar River. The specific conductance in this well appears to fluctuate inversely with the 

water level; as the water level increases, specific conductance decreases. This relation could indicate that 

the water in the Logar River that is recharging this area is less saline during times of high flow than 

during low flow. The high water levels during the period of record generally appear to decline, from a 

maximum of 5.6 m bgs to 6.4 m bgs. The minimum water levels remained fairly constant at about 

7.6 m bgs.

The other GWM in the Logar River valley in the AOI is GWM 17 (fig. 2C–6a

GWM 4, in the Kharuti Dawrankhel subarea, is in the Chakari River valley about 250 m from the 

active river channel. This well is located in the conglomerate sediments and rocks geohydrologic group, 

and the bedrock outcrops that form the hills to the west are composed of the limestones and dolostones 

geohydrologic group (fig. 2C–6

). The water-level 

hydrograph for this well shows fairly regular water-level maximums that are probably related to 

seasonal recharge in the spring and early summer. The water-level minimums occur most frequently in 

the winter. The maximum and minimum water levels during the period of record are fairly consistent. 

The maximums are about 11 m bgs and the minimums are about 14 m bgs. Because this well is about 

2 km west of and 10 m higher than the Logar River, the closest surface-water source, the highs and lows 

could correspond to snowmelt runoff from the hills to the west, which reach elevations of 2,000 m asl. 

The specific-conductance hydrograph generally declines over the period of record. 

a). The conglomerate sediments and rocks are semi-consolidated 

deposits with an estimated hydraulic conductivity of about 1 to 10 m/d (meters per day) (Böckh, 1971; 

Mack and others, 2010). The well is 52 m bgs and has a period of record that extends from 

week 1, 2005, until week 35, 2010. The water-level hydrograph for this well shows an overall rise in the 

water level during the period of record. The early part of the period of record—from week 1, 2005, until 

about week 13, 2006—shows fairly regular water-level maximums that are probably related to seasonal 

recharge (highs in spring and early summer, lows in fall and winter). The later part of the record consists 

of a number of water-level highs and lows that do not correspond to the expected wet and dry times of 

the year in Afghanistan. It is not known whether the water levels were measured during static or 

pumping conditions; however, this well most likely is a hand-pumped well, and the water-level 

measurements probably represent reasonably static conditions. The variability in the water-level 

hydrograph from week 13, 2006, until the end of the period of record could be caused by interference 

from another nearby well that is outfitted with an electric pump. The specific-conductance hydrograph 

for this well follows the pattern of the water-level hydrograph. 
152 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

A 90-m-deep supply well, located in the northeast corner of the Logar Valley subarea, for which 

well-completion and -development information was limited, was assessed by the Omran Consulting, 

Construction and Engineering Company (written commun., 2008). The well has a submersible pump 

that is reportedly set at 76 m bgs and the static water level was 31 m bgs. The water discharge rate for 

the well was 8.6 L/s, with a dynamic water level of 53.7 m bgs (drawdown of 22.7 m). This well is 

located in an ephemeral-stream valley in an area categorized as the “loess and fine sediments” 

geohydrologic unit; however, the well likely is set in the conglomerate sediments and rock 

geohydrologic group, which underlie the surficial sediments. The well log indicates that the 90-m-deep 

well is about 40 m from an existing water-supply well that is reported to be 50 m deep and therefore 

may be subject to well interference. Two other water-supply wells at the northern boundary of the AOI 

(wells 9 and 10, fig. 2C–6a), also likely in the conglomerate sediments and rocks group, had reported 

yields of about 8 L/s; additional information indicates, however, that actual yields were much less than 

1 L/s.

Available information about groundwater in the AOI is very limited and almost entirely 

restricted to information about the occurrence of shallow groundwater. The shallow wells in the AOI are 

constructed mostly in the unconsolidated sediments of the river channel; sands, undifferentiated; and 

loess and fine sediments geohydrologic groups. Some wells are constructed in the conglomerate 

sediments and rocks geohydrologic group. This geohydrologic group is a potential source of 

groundwater in the Logar Valley subarea and the Kharuti Dawrankhel subarea (fig. 2C–6a); however, 

isotopic analyses of groundwater in the Kabul Basin indicate that water in this aquifer may be thousands 

of years old with limited recharge (Mack and others, 2010). Hydrologic investigations, including 

source-water analyses, would be needed to adequately characterize this resource. No lithostratigraphic 

information is available for the one reported deep well in the AOI, but this well probably is constructed 

in semi-consolidated conglomerates. No well information is available for consolidated-rock 

geohydrologic units. The consolidated-rock outcrops cover about 65 percent of the surface of the AOI 

(fig. 2C–6a). The sedimentary rocks and limestones and dolostones geohydrologic groups are potential 

areas for hydrologic investigations including detailed mapping and borehole construction and hydraulic 

testing. The metamorphic rocks and intrusive rocks and lavas geohydrologic groups could also be areas 

for groundwater exploration, although the amount of water contained in these rocks likely is limited and 

highly dependent on local fracturing. It is unlikely that the shallow alluvial aquifers could provide large 

withdrawals without disrupting existing domestic supply and irrigation. Additional hydrologic 

investigations are needed to determine whether large groundwater withdrawals from deep, 

semi-consolidated aquifers are sustainable. Close monitoring and careful management would be needed 

to avoid adverse effects on existing uses of local water resources and to ensure their sustainability. 

2C.2.3 Lineament Analyses

Lineaments are photolinear features that could be the result of underlying zones of high-angle 

bedrock fractures, fracture zones, faults, or bedding-plane weaknesses. Lineament analyses were 

conducted in the Aynak copper, cobalt, and chromium AOI using DEM and natural-color satellite 

imagery (fig. 2C–7) and Advanced Spaceborne Thermal Emission and Reflection Radiometry (ASTER) 

satellite imagery (fig. 2C–8a,b). Lineament identification and analysis have long been used as a 

reconnaissance tool for identifying areas in carbonate bedrock environments where groundwater 

resources are likely to be found (Lattman and Parizek, 1964; Siddiqui and Parizek, 1971). Lineament 

analysis is increasingly used to identify areas of high relative well yields in other bedrock settings, 

including crystalline bedrock (Mabee, 1999; Moore and others, 2002). The lineaments shown in 

figure 2C–7 were delineated visually, whereas those in figure 2C–8 were delineated using an automated 

process and on the basis of the multispectral characteristics of the land surface (B.E. Hubbard, 

T.J. Mack, and A.L. Thompson, U.S. Geological Survey August 24, 2011, written commun.). Water 

wells in bedrock aquifers generally are most productive where boreholes are located in areas of highly 

fractured bedrock. Lineaments provide an indication of areas that warrant further investigation for 
Chapter 2C. Geohydrologic Summary of the Aynak Copper, Cobalt, and Chromium Area of Interest 153

optimal bedrock water-well placement. Lineaments may also indicate areas of preferential flow and 

storage of groundwater, and areas with a high density of lineaments may indicate high secondary 

porosity. Any lineament analyses, including those presented in this investigation, need to be 

corroborated by field investigations and additional data to confirm the nature of the lineaments and their 

relation to water-filled bedrock fracture zones.

Lineament-density maps (figs. 2C–7 and 2C–8) indicate areas of potentially increased bedrock 

fracturing (figs. 2C–5 and 2C–6). Several areas on the west and east flanks of the Kabul Basin have high 

lineament densities. Some lineaments, particularly the 15-m lineament dataset (fig. 2C–8b), follow 

mapped faults such as the Chaman fault on the west side of the Kabul Basin (fig. 2C–5b), which could 

represent areas of high-permeability, highly fractured rock. The Yagh-Darra Gul-Darra and Bakhel 

Charwaz subareas, which are areas with little sediment cover, have areas of dense lineaments that may 

represent rock fracturing. Springs in the areas of mapped lineaments, described earlier in this chapter, 

indicate the potential for limited groundwater storage in fractured rock. A spring was found to originate 

in highly fractured metamorphic rock with little upland area on the north flank of the Yagh-Darra 

Gul-Darra subarea during a period with no recent precipitation. Evidence also was found of a spring 

originating in fractures in sedimentary rock in another area described earlier in this chapter, during the 

same period with no recent precipitation. Figure 2C–9 shows a gully and two linear cuts in a bedrock 

hillside that were identified in the 30-m DEM and natural-color image analysis (fig. 2C–7). Wet ground 

was observed where the lineament intersected the gully, and a small settlement was located 

downgradient along the gully or spring channel in an otherwise sparsely populated area. This finding 

indicates that groundwater resources are present in the fractured bedrock in the area; however, this 

resource may provide only enough water for small-scale uses, and close monitoring would be necessary 

to ensure that any new withdrawals did not adversely affect existing springs and water uses. In 

mineralized areas, water quality and potential changes in quality with use, such as changes in oxidation 

resulting from drawdown, would need to be assessed. 

2C.2.4 Water Quality

Two previous USGS and AGS water-resource studies of the Kabul Basin included a northern 

portion of the Aynak copper, cobalt, and chromium AOI (Broshears and others, 2005; Mack and others, 

2010); the water-quality findings from these two studies are representative of the AOI and are 

summarized here. The major-ion chemistry of groundwater in the Kabul Basin was generally of the 

calcium-magnesium-bicarbonate type. Concentrations of some water-quality constituents in the Logar 

area, as in the central Kabul Basin, were higher than those in other areas of the Kabul Basin. Differences 

in water chemistry in the region indicate possible influences of anthropogenic or industrial 

contamination, poor well construction, possible dissolution of rocks containing gypsum, or increased 

concentrations of ions caused by evapotranspiration processes as suggested by Broshears and others 

(2005). Groundwater in the Deh Sabz basin, about 10 km north of the AOI, which is in a hydrogeologic 

setting similar to that of the Chakari River basin in the eastern area of the AOI, appears to have evolved 

from the calcium-magnesium-bicarbonate type to a sulfate-chloride or sodium type (Mack and others, 

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

Figure 2C–7. Lineaments and lineament density based on 30-meter digital-elevation-model data and natural-color 

Landsat imagery in the Aynak copper, cobalt, and chromium area of interest in southeastern Afghanistan.
Chapter 2C. Geohydrologic Summary of the Aynak Copper, Cobalt, and Chromium Area of Interest 155

a 
156 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

b 

Figure 2C–8. (a) Lineaments and lineament density based on 30-meter multispectral Landsat imagery in the 

Aynak copper, cobalt, and chromium area of interest, and (b) lineaments and lineament density based on 15-meter 

multispectral Landsat imagery in the Aynak copper, cobalt, and chromium area of interest in southeastern

Afghanistan.
Chapter 2C. Geohydrologic Summary of the Aynak Copper, Cobalt, and Chromium Area of Interest 157

Figure 2C–9. Photograph showing small orchard at the intersection of linear features (lineaments) cutting a 

hillside and a small ravine at Zakhel.

The median values of several groundwater parameters, including specific conductance, hardness 

measured as alkalinity, and concentrations of nitrate plus nitrite, bromide, magnesium, sodium, 

potassium, chloride, arsenic, boron, nickel, and zinc, were elevated in densely populated areas. Uranium 

concentrations were higher than 5 μg/L (micrograms per liter) in much of the Kabul Basin; however, no 

World Health Organization (2006) standards for metals, such as arsenic, cobalt, copper, lead, or 

uranium, were exceeded in surface water or groundwater in the Logar River basin (Mack and others, 

2010). Median specific conductance of groundwater ranged from 51 (near the mountains on the west 

side of the basin) to 1,177 μS/cm (in central Kabul). Specific conductance in the Kabul Basin generally 

was higher in densely populated than in sparsely populated areas. Overall, conditions in the aquifer were 

slightly oxic, with dissolved-oxygen concentrations in the subbasins ranging from 0.1 to 1.9 mg/L 

(milligrams per liter) as O2 with a median value of 0.1 mg/L. Median concentrations of nitrate as N

(nitrogen) ranged from 1.2 mg/L at the eastern side of the basin near the mountains to 6.7 mg/L in 

central Kabul. The median concentration of nitrate as N for the entire Kabul Basin was 3.3 mg/L.

Total coliform bacteria were detected in nearly all of the groundwater samples from the Kabul 

Basin. In some wells counts exceeded 2,420 colonies per 100 mL (milliliters). More than 100 colonies 

per 100 mL were detected in samples in all areas of the Kabul Basin except at the eastern side of the 

basin near the mountains (4 colonies per 100 mL). E. coli was detected in 66 of 68 samples collected in 

the Kabul Basin. Water from a well located in the Deh Sabz basin, which contained more than 

2,420 colonies per 100 mL total coliform, had the highest reported concentration of colonies of E. coli
158 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

present (461 colonies per 100 mL). Detections of E. coli appeared to be randomly distributed throughout 

the region. The prevalence of bacteria in groundwater samples likely indicates the existence of 

inadequate sanitation facilities for waste disposal and poor well construction throughout the region. 

These conditions allow sewage effluent to contaminate the wells.

2C.3 Summary and Conclusions

The availability of water resources for mining and other uses is likely to be more limited in the 

Aynak copper, cobalt, and chromium AOI than in other areas of Afghanistan because recharge rates are 

low and surface-water flow is limited. Water resources in the AOI and the surrounding area consist 

mainly of streams, and groundwater in deep aquifers. The Logar River, which flows through the center 

of the AOI, is the primary surface-water resource in the area. The river is used heavily for irrigation and 

local domestic supply, which limits the availability of this resource for additional uses. Close monitoring 

of withdrawals from the river would be needed to ensure the continued availability of this resource for 

existing uses. Some water potentially could be withdrawn from the Chakari River during high flows; 

however, during some periods of the year this river becomes dry. Because the Chakari River originates 

in carbonate rocks in the AOI, its existence indicates the potential for that geohydrologic group to store 

and yield water. In these rivers, spring to early summer is a time of high flow. Surface-water flow in 

these rivers is an important source of recharge for the shallow alluvial aquifers in the river valleys. As in 

many areas of Afghanistan, any additional diversion and use of water from the rivers would need to be 

carefully managed to prevent overuse or degradation of this resource. 

There are more than 2,500 nongovernmental organization- (NGO) installed shallow drinkingwater wells in the AOI. Most of these wells are probably polyvinyl chloride- (PVC) cased tube wells 

with hand pumps that are used to supply water for domestic consumption. Shallow wells completed in 

unconsolidated sediments are concentrated in the Kabul and Logar River valleys. The shallow 

groundwater in the AOI likely is recharged primarily by seasonal leakage from the Logar River and 

irrigated areas. Little information is available about groundwater in deep aquifers in the AOI. Deep 

groundwater resources in the conglomerates likely include a component of recharge from upland areas at 

the sides of the basin; however, this water is likely thousands of years old and of unknown quality and 

sustainability. 

The major-ion chemistry of groundwater in the region is generally the calcium-magnesiumbicarbonate type; however, water quality is a concern in some areas of the AOI, particularly the more 

densely populated areas, where nitrate concentrations are likely to be high and bacterial contamination 

may be present. The amount of water available in the shallow alluvial aquifers in the river valleys 

probably is limited, and additional withdrawals of water for mining activities would likely adversely 

affect the continued availability of local water supplies. Although considerable groundwater may be 

present in the deep aquifers in the AOI, investigations are needed to characterize the quantity and quality 

of this resource, and careful planning would be needed to balance any new groundwater withdrawals 

with existing uses. 

2C.4 References Cited

Abdullah, Sh., and Chmyriov, V.M., eds in chief, 1977, Geology and mineral resources of Afghanistan, 

Book 2: Afghanistan Ministry of Mines and Industries, Afghanistan Geological Survey, British 

Geological Survey Occasional Publications No. 15, 292 p. (Reprinted 2008.) 

Afghanistan Information Management Service, 1997, Irrigated areas, 1:250,000 scale: Afghanistan 

Information Management Service, Afghanistan Shape Files, accessed October 15, 2010, at 

http://www.aims.org.af/.

Afghanistan Information Management Service, 2004, Settlements of Afghanistan, 1:100,000 scale: 

Afghanistan Information Management Service, Afghanistan Shape Files, accessed October 15, 2010, 

at http://www.aims.org.af/.
Chapter 2C. Geohydrologic Summary of the Aynak Copper, Cobalt, and Chromium Area of Interest 159

Akbari, M.A., Tahir, M., Litke, D.W., and Chornack, M.P., 2007, Ground-water levels in the Kabul 

Basin, Afghanistan, 2004–07: U.S. Geological Survey Open-File Report 2007-1294, 46 p.

Bohannon, R.G., 2005, Topographic map of quadrangle 3468, Chak Wardak-Syahgerd (509) and Kabul

(510) quadrangles, Afghanistan: U.S. Geological Survey Open-File Report 2005–1107B.

Bohannon, R.G., and Turner, K.J., 2005, Geologic map of quadrangle 3468, Chak Wardak-Syahgerd

(509) and Kabul (510) quadrangles, Afghanistan: U.S. Geological Survey Open-File Report 2005–

1107A.

Böckh, E.G., 1971, Report on the groundwater resources of the City of Kabul, Report for Bundesanstalt 

fur Geowissenschaften und Rohstoffe (unpublished): BGR file number 0021016, 43 p.

Breckle, S.W., 2007, Flora and vegetation of Afghanistan: Basic and Applied Dryland Research, v. 1, 

no. 2, p 155–194.

Broshears, R.E., Akbari, M.A., Chornack, M.P., Mueller, D.K., and Ruddy, B.C., 2005, Inventory of 

groundwater resources in the Kabul Basin, Afghanistan: U.S. Geological Survey Scientific 

Investigations Report 2005–5090, 34 p.

Danish Committee for Aid to Afghan Refugees, 2011, Update on “National groundwater monitoring 

wells network activities in Afghanistan” from July 2007 to December 2010: Danish Committee for 

Aid to Afghan Refugees (DACAAR), Kabul, Afghanistan, 23 p.

Davis, P.A., 2006, Calibrated Landsat ETM+ Mosaics of Afghanistan: U.S. Geological Survey 

Open-File Report 2006–1345, 18 p., also at http://pubs.usgs.gov/of/2006/1345/. 

Doebrich, J.L., and Wahl, R.L., 2006, Geologic and mineral resource map of Afghanistan: U.S. 

Geological Survey Open-File Report 2006–1038, 1 sheet, scale 1:850,000, accessed Feburary 2, 2010, 

year, at http://pubs.usgs.gov/of/2006/1038/

Homilius, Joachim, 1969, Geoelectrical investigations in east Afghanistan: Geophysical Prospecting, 

v. 17, issue 4, p. 468–487.

.Freeze, R.A., and Cherry, J.A., 1979, Groundwater:

Englewood Cliffs, N.J., Prentice-Hall, 

604 p.

Japan International Cooperation Agency, 2007a, The study on groundwater resources potential in Kabul 

Basin, in The Islamic Republic of Afghanistan: 3rd

Japan International Cooperation Agency, 2007b, The study on groundwater resources potential in Kabul 

Basin, in The Islamic Republic of Afghanistan: 4th Joint Technical Committee, Sanyu Consultants, 

Inc., Kabul, Afghanistan, 12 p.

Joint Technical Committee, Sanyu Consultants, 

Inc., Kabul, Afghanistan, 20 p.

Lattman, L.H., and Parizek, R.R., 1964, Relationship between fracture traces and the occurrence of 

ground water in carbonate rocks: Journal of Hydrology, v. 2, p. 73–91.

Mabee, S.B., 1999, Factors influencing well productivity in glaciated metamorphic rocks: Groundwater, 

v. 37, no. 1, p. 88–97. 

Mack, T.J., Akbari, M.A., Ashoor, M.H., Chornack, M.P., Coplen, T.B., Emerson, D.G., Hubbard, B.E., 

Litke, D.W., Michel, R.L., Plummer, L.N., Rezai, M.T., Senay, G.B., Verdin, J.P., and Verstraeten, 

I.M., 2010, Conceptual model of water resources in the Kabul Basin, Afghanistan: U.S. Geological 

Survey Scientific Investigations Report 2009-5262, 240 p.

Ministry of Agriculture, Irrigation and Livestock and the Afghan Meteorological Authority of the 

Ministry of Transport, 2010,The Afghanistan Agrometeorological Seasonal Bulletin, issue no. 7, 

2009–2010, 26 p., available at http://afghanistan.cr.usgs.gov/documents.php

Moore, R.B., Schwarz, G.E., Clark, S.F., Jr., Walsh, G.J., and Degnan, J.R., 2002, Factors related to 

well yield in the fractured-bedrock aquifer of New Hampshire: U.S. Geological Survey Professional 

Paper 1660, 51 p., 2 pl.

.

National Imagery and Mapping Agency, 1995, Vector map (VMAP1): National Imagery and Mapping 

Agency database, available at http://geoengine.nga.mil/geospatial/SW_TOOLS/NIMAMUSE/

webinter/rast_roam.html.
160 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

Oak Ridge National Laboratory, 2010, LandScan global population database 2009: Oak Ridge National 

Laboratory database, accessed February 1, 2011, at http://www.ornl.gov/sci/landscan/

Olson, S.A., and Williams-Sether, T., 2010, Streamflow characteristics of streamgages in northern 

Afghanistan and selected locations: U.S. Geological Survey Data Series 529, 512 p.

.

Peters, S.G., Ludington, S.D., Orris, G.J., Sutphin, D.M., Bliss, J.D., and Rytuba, J.J., eds., and the 

U.S. Geological Survey-Afghanistan Ministry of Mines Joint Mineral Resource Assessment Team, 

2007, Preliminary non-fuel mineral resource assessment of Afghanistan: U.S. Geological Survey 

Open-File Report 2007–1214, 810 p., 1 CD–ROM. (Also available at 

http://pubs.usgs.gov/of/2007/1214/.

Ruleman, C.A., Crone, A.J., Machette, M.N., Haller, K.M., and Rukstales, K.S., 2007, Map and 

database of probable and possible Quaternary faults in Afghanistan: U.S. Geological Survey 

Open-File Report 2007–1103, 39 p., 1 pl.

)

Siddiqui, S.H., and Parizek, R.R., 1971, Hydrogeologic factors influencing well yields in folded and 

faulted carbonate rocks in central Pennsylvania: Water Resources Research, v. 7, no. 5, p. 1295–1312.

Vining, K.C., 2010, Streamflow characteristics of streams in southeastern Afghanistan: U.S. Geological 

Survey Data Series 508, 104 p.

World Health Organization, 2006, Guildelines for drinking-water quality, 3d ed., incorporating first 

addendum, accessed on February 11, 2009, at http://www.who.int/water_sanitation_health/

dwq/gdwq3rev/en/index.html.