Chapter 5C. Geohydrologic Summary of the Daykundi Tin and 

Tungsten Area of Interest

By Michael P. Chornack and Thomas J. Mack

5C.1 Introduction

This chapter describes the geohydrology of the Daykundi tin and tungsten area of interest (AOI) 

in Afghanistan identified by Peters and others (2007). The AOI is in the Gizab, Day Kundi, and 

Shahristan Districts in Daykundi Province, and the Waras District in Bamyan Province (fig. 5C-1a,b). 

The area is entirely mountainous with the exception of a few areas along major river valleys and some 

rolling plateaus. 

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

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

available are limited. This report summarizes 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. 

5C.1.1 Climate and Vegetation

Climate information for the Daykundi tin and tungsten 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 (2005–11), 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 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. 
Chapter 5C. Geohydrologic Summary of the Daykundi Tin and Tungsten Area of Interest 343

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

b 

Figure 5C–1. (a) Landsat image showing the location of, and (b) place names, stream names, and streamgage 

station numbers in the Daykundi tin and tungsten area of interest in the central highlands region of Afghanistan.

The climate of the AOI is typical of the continental interior mountainous region of Afghanistan. 

The winters are characterized by cold temperatures and substantial precipitation, mostly in the form of 

snow, whereas the summers are warm and dry. Four Agromet stations are located in the central 

highlands region. The total rainfall in the central highlands region for 2009–2010 was 221 to 300 mm 
Chapter 5C. Geohydrologic Summary of the Daykundi Tin and Tungsten Area of Interest 345

(millimeters) (Ministry of Agriculture, Irrigation, and Livestock, 2010). The amount of precipitation 

increases from west to east across the AOI. The Agromet station closest to the AOI is 20 km 

(kilometers) to the northeast, at Panjab, Bamyan Province; however, only precipitation data, and no 

long-term average (LTA) data, are available for this station. The total precipitation recorded at the 

Panjab Agromet station for the 2009–10 water year was 564 mm. The maximum monthly rainfall total 

of 269 mm occurred in May 2010. There was no rainfall in March, June, or July 2010. The Agromet

station closest to the AOI for which 2009–2010 water year and LTA precipitation and temperature data

are available is located in Bamyan, Bamyan Province, about 55 km northeast of the AOI at an elevation 

of 3,200 m (meters) above sea level (asl). Precipitation and temperature data for the Agromet station in 

Bamyan are shown in table 5C–1. 

The maximum temperatures in the AOI during the 2009–2010 water year ranged from 35.5°C 

(degrees Celsius) to 44.8°C (Ministry of Agriculture, Irrigation, and Livestock, 2010). The average 

monthly high temperature at the Bamyan station for the 2009–2010 water year was 19.5°C in July 2010 

and the average monthly low temperature was -3.7°C in December 2009. The LTA high and low 

temperatures at this station are 18.2°C for July and -6.8°C for January. 

The natural vegetation in the AOI varies with elevation. Other factors that affect vegetation type 

are precipitation, soil type and depth, slope aspect, and human activity. Overgrazing has left much of the 

AOI with very sparse vegetation. In the stream valleys, where elevations are low, the natural vegetation 

is azonal riverine (Breckle, 2007). Much of the natural riverine vegetation in Afghanistan has been 

harvested for fuel and building materials (Breckle, 2007, p. 181), and has been replaced by cultivated 

crops and orchards. The natural vegetation on the slopes above the streams is classified as Amygdalus 

Scrublands (Breckle, 2007, p. 161). The higher elevations are dominated by alpine vegetation and are 

classified as “thorny cushions, subalpine and alpine deserts and meadows” (Breckle, 2007). Agricultural

development is present in stream valleys but is limited in upland areas (fig. 5C–2). 

Table 5C–1. Annual, long-term annual average, and long-term average minimum and maximum monthly 

precipitation and temperature at the Bamyan Agrometeorological (Agromet) station, Afghanistan.

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

Precipitation Temperature Distance 

1 1 Long-term average Long-term average Agromet from AOI Elevation 2009--10 Monthly Monthly Maximum station center (m) annual Annual Minimum and Monthly minimum and maximum and and month (km) (mm) (mm) month (°C) mean (°C) month (mm) month (mm) (°C)

Bamyan 55 3,200 207.4 142 0 August 34.3 April –6.8 January 5.3 18.2 July

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).Snow days were recorded at 

all four Agromet stations in the central highlands region. The Agromet station at Panjab recorded a total of 33 snow days 

with a total accumulation of 257 cm (centimeters). The total snowfall for the previous year (September 2008 through August 

2009) was 279 cm. Snow was recorded from November 2009 to February 2010, with February having the most snow days 

and the greatest accumulation. This station is at an elevation of about 2,700 m asl, which is comparable to the elevations in 

the AOI. The snow-depth map for January 2010 (Ministry of Agriculture, Irrigation, and Livestock, 2010, map 7) indicates 

snow in the AOI was from 2 to 30 cm deep. The snow-depth map for September 2010 (Ministry of Agriculture, Irrigation, 

and Livestock, 2010, map 7) shows less than 2 cm of snow in the AOI and at the Panjab Agromet station. It is likely that no

snow was present in the AOI in September, but “less than 2 cm” is the lowest snow-depth category shown on the map. 
346 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

Figure 5C–2. Historical streamgage locations, streamflow estimation points, digitally generated drainage network, 

and irrigated areas in the Daykundi tin and tungsten area of interest in the central highlands region of Afghanistan.
Chapter 5C. Geohydrologic Summary of the Daykundi Tin and Tungsten Area of Interest 347

5C.1.2 Demographics

The population density of the Daykundi tin and tungsten AOI as mapped by LandScan (Oak 

Ridge National Laboratory, 2010) with a pixel resolution of approximately 1 km2 (square kilometer) is 

shown in figure 5C-3. Few areas in the AOI have a population density greater than 500 per km2, and in 

most areas it is less than 50 per km2. One of the larger settlements is the Daykundi Province center of 

Nili (figs. 5C–1a,b); however, the population density of the Nili area is less than 500 per km2

 and 

generally less than 100 per km2. Nili is located in a valley formed by a number of ephemeral streams and 

much of the land area is irrigated (fig. 5C–2). The area with the greatest population density is probably 

Gizab, located at the confluence of the Helmand and Rodi Hordak Rivers (fig. 5C–1b), with a few 

locations having a population density of about 1,000 per km2

5C.1.3 Topography and Geomorphology

. Most of the inhabitants live in small 

farming communities that are located in perennial- and ephemeral-stream valleys. Agricultural 

development in the larger valleys in the AOI is extensive. Agricultural development and settlements 

along the Helmand River in the AOI are limited because the valley is narrow with steep sides that limit

the amount of land available for development. Streamflow data (discussed in the Surface Water section) 

indicate that flow in the Helmand River in April and May could result in seasonal flooding that would 

prevent, or at least limit, development within the flood plain of the river. Another more populated area is 

an area of relatively low relief in the northeastern part of the AOI between the Darrah-e-Qarghajur and 

Punjab Rivers (figs. 5C–2 and 5C–3). The roads in the AOI are mapped as “tracks” (Afghanistan 

Information Management Service, 2007), with only a few bridges that cross perennial streams. 

The Daykundi tin and tungsten AOI is in the central highlands region of the Hindu Kush 

Mountains in Afghanistan. The AOI is mountainous and contains several peaks that are higher than 

3,500 m asl. The highest peak, in the southeast corner of the AOI, has an elevation of 3,511 m asl 

(Bohannon, 2005b). The AOI is located in the upper drainage basin of the Helmand River (WilliamsSether, 2008). The Helmand River flows through the southern part of the AOI. The elevation of the 

streamgage station at Gizab (fig. 5C–1b

The geomorphology of the AOI is a product of fluvial processes and local geology. Stream 

valleys are V-shaped and narrow along most of their lengths (Davis, 2006). Some areas along the 

streams are wide enough to support small settlements and cultivated fields. Areas of settlements and 

agriculture are found at the confluences of stream valleys and large oxbow curves (fig. 5C–2). Lowrelief upland areas are developed in some parts of the AOI. The outcrops of sedimentary rocks form 

steeply dipping ridges, but are of limited extent in the AOI (fig. 5C-4). About half of the outcrops in the 

AOI are composed of metamorphic rocks. Much of the area where these rocks crop out is above 2,500 m 

asl. Many peaks in the metamorphic-rock highlands are more than 3,500 m asl. The area is cut by 

streams that exhibit dendritic drainage patterns, but some long, fault-controlled ridges and valleys also 

are present (Bohannon, 2005a,b).

) on the Helmand River is reported to be 1,325 m asl (WilliamsSether, 2008). The AOI can be described as rugged, mountainous highlands incised by dendritic stream 

valleys. Some of the more deeply incised stream valleys have as much as 800 m of relief. The 

topography of the AOI is influenced by the lithology of the bedrock outcrops and the structural geology

of the region. 
348 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

Figure 5C–3. (on previous page) Population density of the Daykundi tin and tungsten area of interest in the 

central highlands region of Afghanistan.
Chapter 5C. Geohydrologic Summary of the Daykundi Tin and Tungsten Area of Interest 349

Figure 5C–4. (on previous page) Topography and generalized geohydrology of the Daykundi tin and tungsten

area of interest in the central highlands region of Afghanistan.
350 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

5C.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

Daykundi tin and tungsten AOI is in the Upper Helmand hydrogeologic massif of the central 

hydrogeologic folded region. 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 

5C–4 with the underlying topography to allow examination of the geohydrology in the context of relief, 

whereas figures 5C–5a and b show 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 5C–5a 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 

the AOI, ranked from high to low relative hydraulic conductivity (Freeze and Cherry, 1979, table 2.3), 

are “sands, undifferentiated; conglomerate sediments and rocks; limestones and dolostones; sedimentary 

rocks; metamorphic rocks; and intrusive rocks and lavas” (figs. 5C–4 and 5C–5a). 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 covers this AOI is provided by Bohannon (2005a). 

The AOI consists largely of the metamorphic rocks group and, secondarily, the intrusive rocks 

and lavas group (figs. 5C–4 and 5C–5a). Minor outcrops of the sedimentary rocks group and the 

limestones and dolostones group are found within the AOI. Mapped unconsolidated deposits are 

confined to a few areas along the active channels of perennial streams. An area of about 20 km2

 around 

the settlement of Gizab at the confluence of the Rodi Hordak and Helmand Rivers is mapped as sands, 

undifferentiated, with some conglomerate sediments and rocks (figs. 5C–4 and 5C–5a,b). Google Earth

aerial images show evidence of minor alluvial and colluvial deposits along all of the perennial and some 

of the ephemeral streams in the AOI. The alluvial and colluvial deposits are limited in areal extent and 

likely are limited in thickness as well. 

Abdullah and Chmyriov (1977) provide the following general descriptions of the water-bearing 

deposits in the region that includes the AOI: “The aquifer, composed of alluvial-fan and talus deposits, 

occur in the Herat, Sehdara, Dakke-Tundi (Daykundi), Kabul, and Aynak intermontane depressions, in 

the Dashte Nawer Depression, and in numerous intermontane valleys. Water-bearing deposits are gravel, 

shingle, sandy loam and loam totaling in thickness from a few meters in intermontane depressions 

(valleys or basins) in the west to 400 m at Shekar Darah.” There is no evidence of karezes (hand-dug 

water-supply tunnels) in the AOI, probably because the amount of alluvial and colluvial sediments is 

limited. 

The known mineral deposits in the AOI are found in the metamorphic rocks group and the 

intrusive rocks and lavas group. As indicated by Abdullah and Chmyriov (1977), the hydraulic 

properties of intrusive and metamorphic rocks are dependent on secondary porosity due to fracturing. 

Fractures in rocks in the AOI are likely to be found adjacent to faults and at intrusive-rock contacts (fig. 

5C–5a). Several faults have been mapped in the AOI (fig. 5C–5a), and other, unmapped faults likely are 

present in the area as well.

5C.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), 

is shown in figure 5C–2. A network representing likely ephemeral streams, generated with a digital 

elevation model (DEM), also is shown in figure 5C–2. Mapped springs, identified in the Vector Map 

(VMAP1) database (National Imagery and Mapping Agency, 1995), are also shown where present in 
Chapter 5C. Geohydrologic Summary of the Daykundi Tin and Tungsten Area of Interest 351

and adjacent to the Daykundi tin and tungsten AOI. Names of major streams and identification numbers 

for any streamgages and ungaged streamflow estimation sites in the AOI are shown in figure 5C–1b. 

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

b 

Figure 5C–5. (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 Daykundi tin and tungsten

area of interest in the central highlands region of Afghanistan.
Chapter 5C. Geohydrologic Summary of the Daykundi Tin and Tungsten Area of Interest 353

The AOI lies within the upper drainage basin of the Helmand River, which is the largest 

perennial stream in southern Afghanistan. Many perennial tributary streams transect portions of the AOI 

(figs. 5C–1b and 5C–2). Historical streamflow data are available for two streamgage stations within the 

AOI in the Helmand River Basin (Williams-Sether, 2008) (fig. 5C–1b). The Punjab River at Waras 

station (Afghan identification number 4-13, R00-4A) is in the northeast corner of the AOI in Bamyan 

Province. A statistical summary of monthly and annual mean streamflows for this station (WilliamsSether, 2008) is shown in table 5C–2. The Punjab River is a tributary to the Helmand River that 

transects the northeast corner of the AOI. The period of record for this station is from 1 October, 1969,

to 20 January, 1979. The drainage area is 1,710 km2 and the elevation of the station is reported as 2,480 

m asl. The annual mean streamflow for the period of record is 8.54 m3/s (cubic meters per second), with 

a standard deviation of 3.95 m3/s. The annual mean streamflow per unit area for this station is 0.005

m3/s/km2. The highest maximum monthly mean streamflow was 93.6 m3/s in May 1976, and the lowest

minimum monthly mean streamflow was 0.75 m3

/s in July 1971. Statistical summaries of the streamflow 

data that are available for all historical gages in Afghanistan can be accessed at 

http://afghanistan.cr.usgs.gov/water.php

The Helmand River at Gizab streamgage station (Afghan identification number 4-0.000-9M) is 

located in the southwestern corner of the AOI at an elevation of 1,325 m asl. A statistical summary of 

monthly and annual mean streamflows for this station (Williams-Sether, 2008) is shown in table 5C-3.

The period of record for this station is from 19 July, 1971, to 11 March, 1979, and its drainage area is 

20,750 km

.

2

. The annual mean streamflow for the period of record is 111 m3/s, with a standard deviation 

of 28.1 m3/s. The annual mean streamflow per unit area for this station is 0.005 m3/s/km2. The highest 

maximum monthly mean streamflow during the period of record was 563 m3

/s in April 1976, and the 

lowest minimum monthly mean streamflow was 18.3 m3/s in August 1971. Statistical summaries of 

streamflow data for all available historical gages in Afghanistan can be accessed at 

http://afghanistan.cr.usgs.gov/water.php.

The Rodi Hordak is a perennial stream that flows through the western part of the AOI and its 

headwaters are north of the AOI (fig. 5C–1b). The stream valley is deeply incised and meandering in the 

outcrops of the metamorphic rocks, but displays a rectangular pattern in the outcrops of the intrusive 

rocks and lavas. The Ajrestan Rud is the other named tributary to the Helmand River in the AOI (fig. 

5C–1b

Streamflow statistics were estimated for selected ungaged streams that may be prominent in the 

AOI or subareas to provide some probable estimates of flow for these locations. Streamflow statistics, 

presented in appendix 2, were calculated for points S27 and S28 (fig. 5C–1

). The headwaters of the Ajrestan Rud are in the mountains south of the AOI. Other unnamed 

steams flow through or originate in the AOI (fig. 5C–2); flow in these streams is probably much smaller 

than flow in the named tributaries.

b) using a drainage-area-ratio 

method (Olson and Mack, 2011) based on historical flows at streamgage stations in the AOI. Point S27 

is located on the Helmand River and has as a drainage area of 11,568 km2

. The streamflow at point S27 

was estimated using data from the Helmand River at Gizab (Afghan identification number 4-0.000-9M)

streamgage station (app. 2–S27). The mean annual streamflow at point S27 is estimated to be 60.61 

m3/s. Point S28 is on the Rodi Hordak and has a drainage area of 4,331 km2. The streamflow at point 

S28 was estimated using data from the Punjab River at Waras streamgage station (app. 2–S28). The 

Punjab River at Waras streamgage station was selected as the most representative historical gage, on the 

basis of drainage-basin characteristics, for use with this method. The mean annual streamflow at point 

S28 was estimated to be 22.53 m3/s. The seasonal timing of maximum and minimum monthly 

streamflow at S27 and S28 would likely be similar to that at the two stations used to calculate the 

estimates, with high flows in the spring and low flows in the late summer.
354 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

Table 2. Statistical summary of monthly and annual mean streamflows for the Punjab River at Waras streamgage station. 3 [m /s, cubic meters per second]

Maximum Minimum Mean

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

October 5.20 1977 1.65 1972 3.26 1.11 0.34 3.18

November 5.60 1970 1.85 1972 3.21 1.25 0.39 3.13

December 4.19 1977 1.56 1973 2.97 0.92 0.31 2.89

January 6.25 1977 1.33 1973 3.38 1.34 0.40 3.30

February 7.95 1977 1.78 1973 4.17 1.80 0.43 4.07

March 10.7 1977 3.24 1972 5.76 2.63 0.46 5.61

April 53.9 1976 7.73 1971 30.3 13.5 0.45 29.6

May 93.6 1976 3.45 1971 33.9 27.6 0.81 33.0

June 20.5 1976 0.997 1971 7.47 6.27 0.84 7.28

July 5.03 1976 0.753 1971 2.73 1.43 0.52 2.66

August 4.84 1978 1.06 1971 2.54 1.13 0.45 2.47

September 4.50 1976 1.44 1971 2.88 0.88 0.30 2.81

Annual 16.9 1976 3.11 1971 8.54 3.95 0.46 100

Table 5C–3. Statistical summary 3 [m /s, cubic meters per second]of monthly and annual mean streamflows for the Helmand River at Gizab streamgage station.

Month

Maximum Minimum

Streamflow Water year of

(m3/s) occurrence

Mean

Streamflow Water year of

(m3/s) occurrence

Streamflow

(m3/s) 

Standard

deviation

3 (m /s) 

Coefficient of

variation

Percentage

of annual

streamflow

October

November

December

January

February

March

April

May

June

July

August

September

Annual

50.0

61.2

57.3

60.8

102

259

563

543

189

95.3

45.1

46.3

159

1977

1977

1977

1977

1973

1972

1976

1976

1976

1976

1975

1976

1976

28.2

32.2

30.5

32.7

35.7

143

230

137

71.5

30.2

18.3

22.0

76.9

1972

1972

1972

1972

1972

1978

1974

1974

1974

1974

1971

1971

1974

41.3

47.4

46.8

48.0

66.8

186

360

286

119

57.8

34.1

35.0

111

6.56

8.58

8.09

8.42

22.4

39.4

112

142

52.7

22.0

8.87

8.47

28.1

0.16

0.18

0.17

0.18

0.33

0.21

0.31

0.50

0.44

0.38

0.26

0.24

0.25

3.11

3.57

3.53

3.61

5.03

14.0

27.1

21.5

8.99

4.35

2.57

2.64

100
Chapter 5C. Geohydrologic Summary of the Daykundi Tin and Tungsten Area of Interest 355

5C.2.2 Groundwater

Approximately 40 shallow community groundwater-supply wells have been installed near the 

Punjab River in the Daykundi tin and tungsten AOI by NGOs. Information about these wells can be 

found in a database maintained by DACAAR (Danish Committee for Aid to Afghan Refugees, 2011).

Well-depth and static-water-level information is available for most of the wells in this database (fig. 5C–

5a,b). Available well-construction information is limited; however, most of these wells are shallow dug 

wells, generally less than 10 m deep, or “tube” wells (driven wells with polyvinyl chloride (PVC)) 

casing), generally 10 to 20 m deep, constructed with concrete-ring casing. They are typically constructed 

in unconsolidated sediments near stream channels; depth to water generally is less than 15 m. About 

four NGO wells are in Nili and a few are in other areas of the AOI (fig. 5C–5a). It is likely that 

additional water wells are present in the AOI, especially in the larger settlements such as Nili, Gizad, 

and Waras. Figure 5C–5b

One groundwater monitoring well, GWM 54 (not shown in figure 5C–5

shows the height of static water in the casings of the water-supply wells (well 

depth minus static depth to water), which was typically 1 to 3 m. Such shallow wells, with little static 

water, were found to be vulnerable to seasonal water-level fluctuations and to 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). Community supply wells are generally equipped 

with hand pumps. Wells constructed for irrigation may be more likely to have electric pumps, powered 

by generators; however, powered pumps are not common in remote areas because of the prohibitive 

expense of fuel.

a

The geohydrology and climate of the AOI are favorable for recharge of groundwater. The 

alluvial and colluvial sediments in stream valleys and upland basins probably are local aquifers of

limited extent and thickness. The alluvial-colluvial aquifer probably is capable of supplying 

groundwater only for local use and likely would not support large-scale withdrawals for mining 

operations. The largest outcrop area in the AOI is composed of the metamorphic rocks group and the 

intrusive rocks and lavas group. These two geohydrologic groups are potential aquifers in the AOI. The 

water yields of these potential aquifers are unknown, but may be considerable where the bedrock is 

highly fractured; these areas may be indicated by lineaments. The AOI receives about 300 mm of 

precipitation per year, mostly in the form of snow during the winter months. The bedrock units are 

weathered and fractured at the land surface—conditions that are favorable for the infiltration of 

precipitation, including snow melt, into the subsurface. Additional study, including geologic mapping, 

geophysics, and drilling and testing of boreholes, would help to characterize these geohydrologic groups 

as potential aquifers.

), is about 40 km north 

of the AOI boundary and is monitored by DACAAR for groundwater levels and specific conductance. A 

hydrograph of water levels in GWM 54, provided by DACAAR, is shown in appendix 3. The 

hydrograph shows the date in week number and year, the specific conductance of groundwater in 

microsiemens per centimeter at 25°C (μS/cm), and depth to water in meters below ground surface (bgs).

The water level in GWM 54, which likely is constructed in alluvial material, fluctuated about 3 m 

seasonally, with a peak in the spring and a low in the late fall. Specific conductance of the water from 

this well was about 1,400 to 1,600 μS/cm.

5C.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 of the 

Daykundi tin and tungsten AOI were conducted using DEM and natural-color satellite imagery (fig. 5C–

6) and Advanced Spaceborne Thermal Emission and Reflection (ASTER) radiometer satellite imagery 

(fig. 5C–7a,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
356 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

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 5C–6 were delineated visually, 

whereas those in figure 5C–7a,b 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, unpub. 

data, 2011). Water wells in bedrock aquifers generally are most productive where boreholes are located 

in areas of highly fractured bedrock. Areas where lineament density is high (figs. 5C–6 and 5C–7a, b) 

potentially are areas where bedrock fractures are more prevalent than in other areas of the AOI. 

Lineaments provide an indication of areas that warrant further investigation for optimal bedrock waterwell 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. 

The westernmost outcrop of the intrusive rocks and lavas geohydrologic group in the AOI (fig. 

5C–4) exhibits a prominent set of northwest-southeast-trending lineaments (fig. 5C–6) and is partially 

surrounded by a thin band of steeply dipping sedimentary rocks. The fractures in this outcrop have a 

strong influence on the drainage pattern (Bohannon, 2005a,b). Lineament groups are densest in the 

northern area of the AOI, in southern areas of the Darrah-e-Qarghajur stream basin (figs. 5C–6 and 5C–

7a). This area is characterized by metamorphic rocks and has less relief than other areas of the AOI (fig. 

5C–5a); the lineaments generally trend southwest-northeast and likely follow regional bedrock foliation. 

These features may be indicative of highly fractured bedrock with low relief and may represent areas 

where groundwater is available in bedrock. ASTER lineament density is greater in metamorphic rocks in 

some areas along the southeastern boundary of the AOI than in other areas (fig. 5C–7a,b).

5C.3 Summary and Conclusions

Water resources for mining and other uses are likely to be more available in the Daykundi tin

and tungsten area of interest (AOI) than in other areas of Afghanistan. Streamflow estimates based on 

historical records indicate that surface-water resources potentially are available for uses such as miningrelated activities. The diversion of water from the upper Helmand River basin would need to be closely 

monitored, particularly during low-flow periods. The quantity and quality of the water resource need to 

be assessed so that surface-water flow remains sufficient to supply water for irrigation and to provide 

recharge to the aquifers that supply groundwater to the shallow wells for domestic consumption. 

Perennial streams that transect or are within the AOI are also potential sources of water that may support 

mining activities.

The groundwater resources of the AOI are not well known; however, the climate and 

geohydrology of the AOI are favorable for groundwater recharge. The limited areal extent and thickness 

of alluvial deposits in the AOI indicate that the potential for groundwater availability in the alluvial 

aquifers probably is limited. Additionally, the local population is probably highly dependent on the 

shallow water resources in these aquifers. Some areas of the AOI, as indicated by generalized 

geohydrologic maps and lineament analyses, are likely areas for further exploration for groundwater 

resources. The greatest potential for additional quantities of groundwater is in the weathered and 

fractured metamorphic rocks and the intrusive rocks and lavas geohydrologic groups. Mapped 

lineaments, which may indicate faults and associated fractures zones, are likely areas for further 

exploration for groundwater resources. The contact between the intrusive rocks and lavas and the 

metamorphic rocks also may be an area that is promising for groundwater exploration. Lineamentdensity maps indicate that the metamorphic rocks may be more highly fractured than the intrusive rocks 

and lavas. Additionally, shallow saturated zones could be present in the intrusive rocks and lavas in the 

upland basins. The quality and sustainability of water resources in the AOI remain to be determined, 

however. Close monitoring and careful management of potential new surface-water or groundwater 

withdrawals would help to protect the quantity and quality of the existing supply for current local water 
Chapter 5C. Geohydrologic Summary of the Daykundi Tin and Tungsten Area of Interest 357

uses. Field investigations including geologic mapping, geophysical surveys, and hydraulic well testing 

are needed to adequately characterize the extent and availability of groundwater resources in the AOI. 

Figure 5C–6. Lineaments and lineament density based on 30-meter digital-elevation-model data and naturalcolor Landsat imagery in the Daykundi tin and tungsten area of interest in the central highlands region of

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

a 
Chapter 5C. Geohydrologic Summary of the Daykundi Tin and Tungsten Area of Interest 359

b 

Figure 5C–7. (a) Lineaments and lineament density based on 30-meter multispectral Landsat imagery and (b)

lineaments and lineament density based on 15-meter multispectral Landsat imagery in the Daykundi tin and 

tungsten area of interest in the central highlands region of Afghanistan.
360 Summaries of Important Areas for Mineral Investment and Production Opportunities of Nonfuel Minerals in Afghanistan

5C.4 References Cited

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

book 2—Mineral resources of Afghanistan: Afghanistan Ministry of Mines and Industries of the 

Democratic Republic of Afghanistan, Afghanistan Geological Survey, British Geological Survey 

Occasional Publication 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, accessed 

October 15, 2010, at http://www.aims.org.af/.

Afghanistan Information Management Service, 2007, Afghanistan Day Kundi Province map, at 

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

no. 2, p. 155–194.

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

Bohannon, R.G., 2005a, Geologic map of quadrangles 3366, Gizab (513) and Nawer (514) quadrangles, 

Afghanistan: U.S. Geological Survey Open-File Report 2005–1111A, scale 1:250,000.

Bohannon, R.G., 2005b, Topographic map of quadrangle 3366, Gizab (513) and Nawer (514) 

quadrangles, Afghanistan: U.S. Geological Survey Open-File Report 2005–1111B, scale 1:250,000.

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

wells network activities in Afghanistan” from July 2007 to December 2010: Kabul, Afghanistan, 

Danish Committee for Aid to Afghan Refugees (DACAAR), 23 p.

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

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

Doebrich, J.L., and Wahl, R.R., comps., with contributions by Doebrich, J.L., Wahl, R.R., Ludington, 

S.D., Chirico, P.G., Wandrey, C.J., Bohannon, R.G., Orris, G.J., Bliss, J.D., Wasy, Abdul, and 

Younusi, M.O., 2006, Geologic and mineral resource map of Afghanistan: U.S. Geological Survey 

Open File Report 2006–1038, scale 1:850,000, available at 

Freeze, R.A., and Cherry, J.A., 1979, Groundwater: Englewood Cliffs, N.J., Prentice-Hall, 

604 p.

http://pubs.usgs.gov/of/2006/1038/.

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., and others., 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

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 Mack, T.J., 2011, Technique for estimation of streamflow statistics in mineral areas of 

interest in Afghanistan: U.S. Geological Survey Open-File Report 2011–1176, available at 

.

http://pubs.usgs.gov/of/2011/1176/.
Chapter 5C. Geohydrologic Summary of the Daykundi Tin and Tungsten Area of Interest 361

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.

)

Safi, Hassan, 2007, Groundwater monitoring, Evaluation of groundwater data: Kabul, Afghanistan, 

Danish Committee for Aid to Afghan Refugees, 99 p.

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.

Whitney, J.W., 2006, Geology, water, and wind in the lower Helmand Basin, southern Afghanistan: 

U.S. Geological Survey Scientific Investigations Report 2006-5182, 40 p.

Williams-Sether, T., 2008, Streamflow characteristics of streams in the Helmand Basin, Afghanistan: 

U.S. Geological Survey Data Series 333, 341 p.