^ . t

Report Wo. IAEA - R - 362O--F

TITLE

Study of the intei—relation between shallow and deep aquifers in Valley, Pakistan

FINAL REPORT FOR THE PERIOD

1 December 1983 - 31 December 1986

AUTHOR(S)

M. Ishaq Sajjad

INSTITUTE

Pakistan Institute of Nuclear Science and Technology, Rawalpindi, Pakistan

INTERNATIONAL ATOMIC ENERGY AGENCY

DATE April 1987 STUDY OF THE INTERRELATION BETWEEN SHALLOW AND DEEP AQUIFERS IN MARDAN VALLEY-PAKISTAN

FINAL REPORT

IAEA Contract Nos 3620/RB Principal Investigator! M. Ishaq sajjad

Co-Investi gators: S.D. Hussain, M.Ahmed, ñ.A. Tasneem,R.M. Qureshi and W. Akram. Per i od: Dec.1983 to Dec.1986

Institutes Pakistan Institute of Nuclear Science ?< Technology, Ni lore, Islamabad- Pakistan STUDY OF THE INTERRELATION BETWEEN SHALLOW AND DEEP AQUIFERS IN MARDAN VALLEY-PAKISTAN

The area on the west side of the river Indus includes the districts of Mardan, Peshawar, Kohat, Bannu and D.I.Khan and consists of small valleys, generally surrounded by low, erodable hills. The biggest valley is that of the Mardan district. Its 4 gross area under irrigation constitutes at 19:; 10 hectares. It is surrounded by low hill ranges of Swat and Khyber. The valley fills are formed of erosion from the low hills. The prosperity of the project area depends on the availability of irrigation water supply from the Swat River. The lower Swat Canal was taken out from Munda Heaclworks in 1890. Another canal, called the Upper Swat Canal, was taken out of the river Swat at Amandara in 1915. It crosses the ranges of Malakand hills through a tunnel, and irrigates large areas lying to the East of Mardan.The canal infi Iteration has resulted in a serious problem of waterlogging on the law lying areas. At some places water can even be seen at the surface.

Groundwater occurs largely in two sones: i) a shallow unconfined zone and ii) a deep confined zone. The shallow groundwater zone receives its recharge directly from irrigation channels and rainfall. The low permeability and generally large thickness of the deposits underlying this zone restrict sub- surface drainage and create a high water table condition over a considerable area. Considering the artisian pressure associated t.

with the confined ¡zone, a detailed isotopic study is intended ta determine the significance of upward leakage and its role in the creation of waterlogging problem in the Mardan valley (1).

2- SiQyYDBQLQQY QF THE fiBEfij. Soils near the foot hills are generally piedmont type and formation contains extensive stratifications. The deposits vary at each site. Shingle beds are also found and water-bearing sand formations are comparatively less <1>. The project area occupies the Mardan plains and is predominantly underlain by few hundred meters of unconsoli dated pleistocene and recent deposits of alluvial and aeolain sources. These deposits overlie a consolidated bedrock basement of early mesozoic and other rocks, which outcrop at a number of localities in the plain area and form hills and high mountain ranges off the northern project's boundary.

Information on the lithologie characteristics of the unconsoli dated deposits is available from lithologie logs of test boreholes drilled by the Water and Power Development Authority (WAPDA) between 1968 and 1977. The total thickness of the unconsolidated deposits is not known as none of the test boreholes was deep enough to penetrate the entire thickness of these deposits. The data available for the upper 350 m or so, indicate that unconsoli dated material consists of predominantly fine clay, silty clay, and silt deposits interbedded with discontinuous alluvi«! sand and less commonly, gravel layers of varying thickness. In much o-f the project area groundwater occurs in two zones; a shallow unconfined zone of low permeability, consisting o-f silt, clay, and occasionally fine sand beds, and a deep and gener¿í.lly confined zone of variable but locally high permeability, consisting of sand and gravel beds ranging in depth of less than 35 m to more than 150 m. These zones are often separated by large thickness of fine clay deposits of low permeability. The water level contours and the general direction of groundwater flow in the unconfined shallow zone generally conform to the land surface contours.

The shallow zone receives its recharge from canals, rainfall and irrigation practices. The low permeability and generally large thickness of the deposits underlying this zone restrict subsurface drainage and create a high water table conditions over a considerable arma of the project. This is particularly manifested in the central region, where water table is within 2 m below land surface in about 2/3 of the total area and within 4 m in the remaining area. It is believed that deep zone receives its recharge from bedrock outcrop areas. The areas bordering the mountain front on the nothern boundary of project area are potential recharge areas for this zone. There is lithologie and hydrologie evidence that the deep aquifer is essentially confined. This aquifer is overlain by considerable thickness of clay and silt deposits over much of the project area. These deposits have low permeability and ar& of sufficient thickness to from an aquielude overlying the aquifer.

The hydrostatic head in the deep zone is different from that in the shallow zone. A water level hydrograph of shallow and deep observation wells along the Charsada-Mardan road illustrates that the hydrostatic head in the deep zone is lower than that in the shallow zone« In other parts o-f the area the hydrostatic head in the deep zone is higher than in the shallow zone <2) .

3- CLIMATE OF IHE AREA The area has a subtropical and semi-arid climate. Summers are hot and dry in June and very humid in July & August. Winters are relatively cold with light -frost in December and January. The o mean monthly maximum and minimum temperatures range -from 18 C to o o o 40 C and 4 C to 27 C respectively. Rain-fall occurs both in summer and winter, the total being about 400 mm. The meam altitude o-f the area is 333 m above sea level.

The location map o-f sampling points such as open wells, canals and tubewell s spread over the entire area is given in Figure 1« A number o-f water samples have been periodically collected from the area during the last three years. Teamperature, pH and electrical conductivity measurements were made in-situ. The two canals namely; the Upper Swat and the Lower Swat were sampled on monthly basis. The results based on these analyses are as -follows:

SlôIUi 11QIQEII BE iBBUNDW 18 18 SD-60 plot and frequency distribution of SO data for three sampling periods and that of the entire period i.e. July 1982 to April 1986 (on quarterly basis) are given in figures 2-8. The isotopic data has a spread along the Global Meteoric 18 Water Line ÍGMWL) Bd = BO + .10. Most o-f the isotopic data especially with depleted oxygen values lie above the meteoric line. A few samples show evaporation ef.fect. The depleted samples have deuterium excess higher than 10 while the heavier ones have around 10.

The frequency distribution (figures 5,6,7) has a spread of IB SO values from -13.0 to -4.5 V.o. However, most of the samples 18 lie in the range of -9.5 to -5 V.o. Figure 8 (a) and 8

4.2. ISQigPIC INDEX OF ÇANâU §Y§IEM Both the Upper and Lower Swat canals are fed by the river Bwat. The Upper Swat canal has been sampled on monthly basis at sampling point No. 51 (see Figure 1). The sampling of Lower Swat canal has also been done at various paints but every 3 to 4 months. The Isotopic contents are similar to those upper of Swat Canal.

The monthly isotopic data of the canal system show strong 18 variations in SO ranging from -7 to -12 %o as shown in 18 figure 9. The weighted mean of 80 for the year 1983-1986 is -9.0 %o. The strong isotopic variations indicate that the river is not fed only by a single source rather two or more sources such as snow—melt and rains at high mountains contribute different proportions at different times. It is interesting to nat.3 that the most depleted peak is usually observed at the sampling point No. 51 in the months of June - August (-figure 9). It is most probably due to snow-melt and heavy rains uphills.

4.3. DEUTERIUM EXŒS8 18 The deuterium excess1 d' == 8D - 8 60 is a geographic effect on the stable isotope content and in this case has variations •from S to 20 V.o in shallow and deep groundwater. Its frequency distribution is depicted in figure 10.

The deuterium excess in canal water varies from 12 to 26 V.o, 18 and BO from -7 '/.a to -12 %o as is shown in figure 11 and figure 12 respectively. It is noted that the most depleted values have higher deuterium excess showing the major contribution to the canal system from the snow-melt at higher mountains. The mean value of 'd' is about 19 Jio. The value of deuterium excess for rain samples is 9.5 V.o

4.4. SPATIAL DISTRIBUTION OF Qrl§ 18 The BO values of shallow and deep wells have been given in the figure 13. In the north (top of the figure), usually depleted 18 BO values in the range -7.6 to -9.5 V.o are found. In the lower part of area between lower Swat canal and Kabul river, values in the range of -5 to -7 V.o are dominant. Similarly central area bounded by Mâchai Branch, Jaganat Branch and Gadar Khwar has also 18 BO values in the range -5 to -7 V.o. In these two areas depleted 18 BO values are usually associated with high tritium values. In 18 the South-East corner, sampling points are depleted in 0 except for the open well Mo. 57. The sampling point No. 59 (open well) is .ta" most «depleted isotópica! ly. Its 0 values range from -12.8 to -10 V.o with a moan value of -11.4 +/-• 0.8 "/.a . Spatial 14 distribution of C is depicted in figure 14.

4-5. IBÍIIÜO UÛIÙ Tritium contents alongwith «sampling points have been depicted in figure 13 « The shall o w a qu i fer h a s u s u a11 y h i g h t r i t i um va1u es (49 t o 150 TU) whereas the deep aquifer (tube wells) has lower tritium content in the range of 0-17 TU. However, there are some exceptions too. Shallow wells 26S, 28S, 40S, 46S, 69S, 70S and 81S have tritium contents: 18, 15, 14, 10, 8, 8, and 9 TU respecta, veil, y whereas deep wells 29, 36, 44, 56, 53 and 60 have high tritium values in the range of 45 to 150 TU. The tritium content of canal water sampled at three different times has a mean value of 50 +/- 5 TU.

4.6. ISgiQPIÇ DAJ.A OF PRECIPITATION The isotopic data of the adjacent Peshawar valley is given 18 in Tab.1.e--l. The weighted mean for the year 1983 is SO ~ --5.0 V.o, SD = --30.7 V.o. The mean deuterium excess is 9.5 V.o. It clearly indicates that the local rains lie on the worldwide meteoric line 18 SD ~- 8 SO -i- 10. Rain samples collected from Mar dan city have been analysed and arts very similar to those of Peshawer valley.

4.7. CARBON ISQIOPES i Ç=13 and Ç=14 i Each of the important recharge areas have characteristic

8 13 14

BC values. Similarly radiocarbon (C ) can be used to delineate

the intake areas. The dissolved inorganic carbon content o-f

groundwater could be due to the sources (3) such as:

a> atmospheric carbon dioxide dissolved in rainwater.

b) carbon dioxide produced by the decomposition of organic

matter in the soil or by root respiration in the

unsaturated soil zone.

c) solution of carbonate minerals in the unsaturated and

saturated zone.

d) oxidation of the organic matter present.

e> reduction of sulfate by inorganic material present. 13 14 Water samples for C and C were collected from the area 13 and their contents have been determined. 6C values have variations in the range:

Shallow waters: -5.2 V.o to -12.8 '/.a Deep waters: -4.8 Y.a to -10.5 Xo Canals: -6.2 %o to - 9.0 '/.a

14 C values range from 50 pmc to 135 pmc for shallow and deep aquifers.

4.8. Phv.»i.o-Ch§!!!!Í.!=§L üñtñ

Analysis for Na, K, Ca, Mg, Cl, CO , HCO , NO and SO has 3 3 3 4 been made and the results are given in Table 2.

Electrical conductivity (EC) measurements indicate that the groundwater salinity in the unconfined shallow aquifer is somewhat higher than the underlying confined aquifer. The range of EC in the shallow zone is 500 uS to 2300 uS and that o-f the deep zone 350 uS to 800 u5. The pH values range from 7.0 to 8.5 . EC and pH of canal system measured at various points range from 50 to 9a uS and 7.8 to 8.5 respctively. Temperature of the o deep zone ranges from 22 - 27 C whereas relatively large temperatures variations are observed in the shallow zone.

4.9. WAT.ER LEVEL CONTOURS From the recent (1984) available water table data, contours have been drawn and depicted in figure IS. The water level contours and the direction of groundwater flow in shallow zone generally conforms to the land surface contours.

5. DISCUSS 1QN.S 18 The weighted mean BD of the upper Swat canal from the monthly data over the year 1983-86 is -9.0 "/.a. The deuterium excess is 19 V.o. This higher deuterium excess is due to the Mediterranean and similar marine befts of rapid evaporation. Considering the location of sampling points 12S and 13S, one can easily imagine that their source of recharge is only Lower Swat canal. These have tritium contents of 57 TU. The oxygen isotopic index of rain as given in Table-i. is -5.0 %o with a deuterium excess of about 10 V.o. Looking at 18 histograms (figures 5,6,7) of BO , one finds that sampling point 68S staying in the same position even after long time. It has a 18 mean BD = -5.0 +/- 0.2 '/.a and SD - -32.0 +/- 3.0 V.o. Its tritium contents are about 50 TU. Keeping in view its location

10 (away from the canal) one can consider it to be recharged only by the local rain. Also its isotopic inde;-: is identical to that of rain in Peshawar valley for the year 1983. There-fore, the istopic values o-f this sampling point can be used as a representative rain index. ^

The isotopic index of precipitation over the bedrock outcrop i.e. areas border i nig the project area along the northern boundary

would have similar tritium contents but a little more depleted 18 la BO value than the project area (SO = -5.0 V.o) due to the altitude effect. The magnitude of such altitude effect depends 18 on local climate and topography, with gradients in 0 between 0.2 — 0.5 V.o per 100 meters. Using an. estimated value of 0.2 V.o 18 per 100 meters for an 0 gradient for this area, the isotopic

index of precipitation an the bedrock outcrop amounts to be -5.6 V.o. Having identified the various isotopic indices of input sources, the isotopic data of the groundwater can be evaluated. The deep confined aquifer overlain by clay is believed to receive its recharge from the bedrock outcrop and the areas bordering the mountain front along the northern boundary of the project area (2). The oxygen isotopic index of 12 deep wells having tritium values in the range of 2 ~ 20 TU is -5.7 +/- 0.2 V.o. This value is the same as determined for the areas recharging the confined aquifer.

Other deep wells having tritium values between 20 - 57 TU receive small proportion of their recharge from canals (canal 18 3 index: BO = - 9.0 "/.05 1-1= 57 TU). Figure 16 shows such a mixing pattern i.e. with the increase in tritium (above 20 TU) the

11 oxygen isotopic index gets depleted. The deep wells having tritium more than the canal Eystem (57 TU) have been recharged after 1961-62 when weapon tests* were made. 18 The majority o-f the open wells have 80 in the range o-f -5.0 to -10.0 */.o indicating that these get different proportions of their recharge from rain and canal system (figures 5,6,7,8a). 18 The 80 and the Cl relation for open wells given in figure-17 indicates that these wells have considerable evaporation effect. No such effect is found in deep wells (see figure-18). Some of the open wells have tritium contents below 20 TU and 18 SO in the range of -5.5 to -8.0 "/.o. This indicates that these

receive their rechrge from the deeper zone due to the upward leakage alongwith the small proportion of the canal system. 14 18 C alongwith tritium and 0 delineate this aspect claarly. 18 3 Sämling point 69S (open well) has SO = -6.2 "/o, H= 8 TU and 14 C =57 pmc clearly indicating an upward leakage from deep aquifer. It receives about 80 "/. of its recharge from deeper

confined aquifer which is fed by precipitation on the bedrock 18 outcrop (B0 = -5.6 Y.a) and 20 7. from the canal system. Similarly nearby open wells 70S and 71S receive most of their recharge from deeper aquifer due to the upward leakage. Other sampling points where the upward leakage has been detected are: 81S, 28s, 26S, 40S, and 46S. 14 Figure 19, 20 and 21 showing variations of C with IB 13 3 14 SO , SC and H indicate thst an increase in the C content is 18 associated with depleted 0 values (canal index- -9.0 %o),

12 13 depleted C values (due to the biogenic activity in the shallow sons) and higher tritium contents which are characteristic of the shallow zone.

As regards to the residence time, isotopic data is IB indicative to some extent. The variations o-f 0 with time at different sampling points are relatively small indicating that there is no quick movement of groundwater. Samples having tritium content above 1 TU date the water to be of subrecent age (younger than 50 years) or more likely consist of a mixture of 14 3 older and recent water. Using a combination of C and H data (4,5) we can provide age limits for the Mardan Valley. Samples 14 (or areas) having C contents of 130 pmc together with a tritium content of 100 TU certainly point to a recent water. Values around 50 pmc and low tritium (close to zero ) refer to waters older than 50 years.

Sampling point 59S (open well) has quite a different 18 isotopic index as compared to the rest of the area. Its mean 80 value is -11.4 V.o with variations from -10 V.o to -12.8 "/.o and tritium content is about 50 TU. The excess deuterium varies from 18-24 V.o. It receives its recharge either from the Kabul river 18 or from the Indus river which are known to have very depleted 0 contents. The lithology of the area and the water table gradient based on the water table contours do not support the idea that the open well 59S is fed by the Kabul river. Therefore it is believed that it gets recharged by the Indus river.

From the isotopic and hydrochemical studies in Mardan valley, the following concluions can be? drawn:

a) Water—logging in the area is mainly due to the irrigation

canal system. However,in some zones the upward leakage

•from the deep con-finer! aqujfer also contributes to this

effect.

b) There is no quick movement of groundwater in the area

and the residence time is in the order of tens of years.

c) Quality of deep groundwater is better than that of the

shal1ow groundwater.

AÇKNQWLEDGEMENIS Authors are grateful to the International Atomic Energy Agency-Vienna for partly providing- technical assistance under the project PAK/3Ó20/RB in the -form of scientific supplies. All expences for field work and isotopic analysis were met by PINSTECH. The keen interest taken by the Director F'INSTECH and the P.A.E.C authorities is acknowledged with gratitude. Thanks are also due to Mr. Iqbal Hussain Khan, Mr.Zahid Latif and other colleagues at the Institute for their help in laboratory work throughout this study and in preparation of this manuscript .

Special thanks &re due to Dr. Peter Frits < University of 14 Waterloo, Canada) for the C analysis of eight carbonate samples. Special thanks are also due to the WAPDA-Hydrogeology Directorate Peshawar and to the WAPDA-C.M.O. Peshawar for providing hydrogeological data for the Mardan valley.

14 REFERENCES

1. Ahmed, IM. (3,974). "Groundwater Resources of Pakistan" Rippon Printing Press Lahore- pakistan.

2. Siddiqui, M.R. (1972). "Groundwater Hydrology o-f Mardan

" Unpublished report by WAPDA-- Lahore, Pakistan. 14 3. Mook, W.G.,(1980). "C in Hydrological Studies" In Handbook of Environmental Isotope Geochemistry, Vol . I, Chap. 2,(Eds. Frits, P. and Fontes», J. Ch. ) , Elisevier, Amsterdam. 4. Ericksson, E., 1962. "Radioactivity in Hydrology". In. H. Israel and A. Kretas (Editor«») , "Nuclear Radiations in Geophysics ",Springer-Verlog,New York, N.Y., pp 47-60. 5. Geyh,M.A.,1972. "On the determination o-f the dilution factor of graundwater". Proc. 8th Int. Conf. Radiocarbon Dating, New Zealand , 1972, pp 369-380.

15 Table 1

Istopic Index of Precipitation in the Peshawar Valley Area in 1983.

Total monthly Month Rain Events Monthly Average -fc Precipitation (mm) 8 (i) (n) S o! SD, i

January 1 22.1 .. -5.4 -33.5 February 5 66.7 -7.9 -51.4 March 10 54.3 -0.5 -12.6 July 1 39.5 -3.5 -15.2 August 17 167.6 -5.8 -32.5 September 1 40.1 -5.2 -31.7

November 2 16.5 -3.6 -21.6

18 Weighted mean 6 0 = -5.0 %; Weighted mean 8D = -30.7 %i Table 2

Average Chemical Data of Water Samples Collected from Mardan Valley During January, 1984 and March, 1985.

Sample No. Na K Ca Mg Cl CO3+HCO3 NO 3 SO4 (PPM) (ppm) (ppm) (ppm) (ppm) (ppm) (ppm) (ppm) MRN-1 53 5 15 17 23 231 1 10 MRN-2 55 4 3 18 4 270 1 31 MRN-4(S) 133 1 7 33 9 479 2 32 MRN-5 64 4 3 17 5 231 2 7 MRN-7 38 4 5 , 38 3 - - - MRN-8(S) 358 26 8 * 7 2'5 357 614 16 405 MRN-9 29 4 7 20 5 209 5 11 MRN-10(S) 17 2 15 7 5 160 13 11 MRN-11(C) 8 2 10 22 ' 15 143 3 13 MRN-12 6 2 16 5 3 - - - MRN-13(S) 9 1 16 6 5 33 2 10 MRN-14(S) 48 3 5 52 72 363 20 9 MRN-15(S) 9 1 15 32 3 279 3 8 MRN-16(S) 28 1 19 19" -• 26 274 4 12 MRN-17(S) 61 1 46 34 T - - - MRN-18(S) 6 2 7 5 9 108 3 7 MRN-20 162 2 12 23 21 223 33 51 MRN-23 45 4 37 42 22 274 3 55 MRN-24(S) 38 5 10 37 9 299 7 17 MRN-25 102 1 11 35 13 - - - MRN-27 223 2 12 6 42 291 20 67 MRN-28(S) 219 1 30 55 66 422 2 193 MRN-29 212 6 4 31 7 - - - MRN-3KS) 156 2 13 22 13 467 10 54 MRN-32 159 6 5 ' ' 15 70 338 1 9 MRN-33 79 3 10 10 21 242 4 11 MRN-34(S) 99 5 18 32 33 400 4 75 MRN-35 37 5 30 20 9 219 2 7 MRN-36 40 3 18 18 7 158 1 10 MRN-37 47 4 37 19 18 235 2 12 MRN-38 43 4 - 12 13 - - - MRN-40(S) 50 20 34 30 33 357 14 31 MRN-41 33 7 30 18 13 227 1 8 MRN-42 37 3 21 16 60 180 3 12 -2-

Sample No. Na K Ca Mg Cl CO3+HCO3 NO 3 (ppm) (ppm) (ppm) (ppm) (ppm) îppm) (ppm) (ppm) MRN-43 35 3 4 24 8 248 2 12 MRN-44 52 3 21 21 8 283 3 15 MRN-45 37 3 33 20 8 297 1 10 MRN-46(S) 81 3 15 39 26 382 - 61 MRN-47 46 9 32 • 24 10 239 3 15 MRN-50 28 5 23 . 13 % 8 183 10 10 MRN-52 32 3 7 "26 4 - - - MRN-53(S) 81 4 49 33 74 358 49 68 MRN-54(S) 60 6 21 29 22 266 5 79 MRN-55 87 11 8 9 27 - - - MRN-56 32 10 46 25 5 236 1 32 MRN-57(S) 114 5 34 15 265 349 11 71 MRN-58 34 8 39 19 4 • 253 6 49 MRN-59(S) 20 7 41 19 11 217 1 48 MRN-60 14 3 5 19 2 - - MRN-6KS) 20 2 1 24 3 - - - MRN-62 40 3 3 21 64 - - - MRN-63(S) 46 1 1 10 1 - - - MRN-65 39 5 31 24 27 231 6 19 MRN-67(S) 51 7 5 26 17 - - - MRN-68(S) 353 10 30 55" " 445 498 16 207 MRN-69(S) 89 3 8 21 365 - - - MRN-70ÍS) 338 2 14 23 245 237 28 216 MRN-73(S) 221 4 11 33 150 - - - MRN-75(C) 246 4 13 25 30 571 3 19 MRN-76(S) 35 5 20 29 25 - - - MRN-77(S) 90 12 27 40 14 432 5 53 MRN-78 90 4 13 18 36 - - - MRN-79(S) 37 57 3 15 13 - - MRN-80(S) 98 3 12 33 40 - - _ MRN-8KS) 547 7 14 49 96 - - MRN-82 517 6 22 35 84 - - - MRN-83 30 7 28 22 7 277 - 19 MRN-85 27 5 10 11 5 - - - MRN-90(S) 130 5 6 43 16 LEGEND

SCALE TUBEWELL . OUGWELL o CANAL SAMPLE 1 NALA s; CANAL TOWN/VILLAGE •

FIG. 1 LOCATION OF SAMPLING POINTS IN MARDAN AREA. 6 O18 (%•) - -K -13 -12 -11 -10 -9 -8 -7 -6 -5 -U -3 -2 -1 0 1 | i i • '• ' ...1 ... 1 1 ' ' I,

f CASED WELLS-—» -10

OPEN WELLS « CANALS A - -20 y • yo - -30 ooy1

• o %of ** s - -i.0 o,o q/ ° • / kkk / - -50 0 >^ S D %• \/ - -60

- -70

- -80

0 y/

- -90

FIG. 2 S O8 VERSUS SD PLOT OF SHALLOW AND DEEP WVTER IN MARDAN VALLEY, NOV. 1982. s o18( %. ) -14 -13 -12 -11 -10 -9 -8 -7 -6 -5 -4 -3 -2 -1 0 i i i i i i i i i i i i o

CASED WELLS • «> yf -10 OPEN WELLS « cp/ CANALS -20

-30 • »or

O O# mOpf O -40 o ooo • / o ooooo« »/

o o o S -50

-60

-70

0 y' -80

-90 / FIG. 3 SO18 VERSUS SD PLOT OF SHALLOW AMD DEEP WATERS IN MARDAN VALLEY, MAY 1983. S O13 (•/..) -u -13 -12 -11 -10 -9 -8 -7 -6 -5 -A -3 -2 -1 i I » t I i i i i I i i i i Ö

CASED WELLS- — -10

OPEN WELLS o -20 CANALS à

-30

-í.0

SDV oo -50

-60

-70

- 80

- -90

FIG. ASOO18 VERSUS SD PLOT OF SHALLOW AND DEEP WATERS IN MARDAN VALLEY, JAN. 19 84 CASED WELLS - •—• 13 OPEN WELLS - —o 12 CANALS 11 11

LO 10 CO 9

8 o 7- A A o 6 CO CO 5- Canal Index, A o o Q ( -9.55 ) ! o o Rain índex S 4 er o o o o »f 3 m o o O o 2 o o MRN-59(S) 68(5) Lu o o o o 1. S A A o o -12-0 -11-5 -110 -105 -10-0 -9-5 -90 -8-5 -80 -7-5 -70 -65 -60 -55 -50 -4-5 -40 18

FIG. 5 HISTOGRAM OF S O18 VALUES OF WATER SAMPLES COLLECTED IIN F\UV« IJÜZ . (Isotopic data of canal is on monthly basis for the full year) CASED WELLS •

13 OPEN WELLS o CANALS A o IRVA l o o 10 i/) V) A o o o o < 9 Rain index A o ü o • A o o o • O AC H IU ' o o o • O • O 5 6 Canal Index (-9,55 ) ¡ o o o • O • O * * A o o o • o • O /ATI O £r LÜ A A o o • • • • • m 3 ^68(S) o MRN-59(S) A o o 2 • r fe o A o o o 6 ci 1 A A A A o • • o o -12,0-11,5 -11,0-10,5 -100-9,5 -9,0 -8,5 -8,0 -7,5 -7,0 -6,5 -6,0 -5,5 -5,0 -4.5 . R n18 1rIG. 6 HISTOGRAM OF SO18 VALUES OF WATER SAMPLES M (Isotopic

OPEN WELLS o Í2 CANALS.... A ce 11 LIN I ü O 10 m O o S 9 o O O o Canal Index Priín ' \r\r\f\\* 8 O A A O o • LU A A o 0 O • o ¡ * ' * i* Z c A o A o o O o 2 • O i— A o 0 o o o 0 • o it CCi 0 o o o o # 0 m LU • 10 m /"» n o 68(S) /MRN-591S) 2 i LL A O o ó O 1 * A A A O o -120 -11-5 -110 H05H00 -9-5 -<3-0 -1î-5 - 80 -7-5 -7-0 -6-5 -60 -56 -5-0 -45 -4-0 B. f 18 *^ O o FIG. 7 HISTOGRAM OF ,5 0 VALUES OF WATER SAMPLES COLLECTED IN JAN. 1984.

FIGURE 8a HÍSTOGRAU OF DELTA 0-18 OF WATER ' "•: SAMPLES FROM OPEN VEILS - JULY 1982 - APRIL 1986 {QUARTERLY SAMPLING)

DELTA 0-IB

FREQUENCY (n)

FIGURE 86 HISTOGRAM OF DELTA 0-L8 0i" SAMPLES FROM DEEP WELLS JULY 1982 - APRIL 1986 {QUARTERLY SAMPLING)

-12 -ii -ie 0-18 # DELTA 0-18 -1 FIGURE 9: VARIATION OF DELTA 0-18 OF CMM¿ SAMPLES

{1983 - 19Ö6) -2

WEIGHTED MEANS .

-3 DELTA 0-18 = -9 7».

m -4 DELTA H-2 = -53 %.

-5 d-EXCESS = 19 %.

-6

-8

, .•-•:.- ^ ' .3* ' m

-9

-10 - 1983-84 - 1984-85 1985-86 -11 —

-12

-13 May Jvn Jul Aug Sej> Oct Nov Dec Jan Feb Mar Apr TIME ' FREQUENCY{n) r— FIGURE 10a. HISTOGRAM OF DEUTERIUM EXCESS SAMPLES FROM OPEN WELLS. JULY 1982 - APRIL 1986 (QUARTERLY SAMPLING)

55

se

•5

40

Ï5

sa

23

za

15

ie

s

DEUTERIUM EXCESS

FREQUENCY (n)

. FIGURE 10b. HISTOGRAM OF DEUTERIUM EXCESS SAMPLES FROM DEEP WELLS. . • JULY 1982 - APRIL 1986 (QUARTERLY SAMPLING)

12 1« 2« 24 2« DEUTERIUM EXCESS FREQUENCY (n) r-FIGURE 11: HISTQCRAk OF DEUTERIUk EXCESS OF CANAL ( URN-51C ) {MAY 1983 - APRIL 1986)

WEIGHTED MEANS DELTA 0-lfl = -9.00 %o DELTA D = -53.00 %o D.EXCESS = 19.00 %o

12 i* 28 24 28 DEUTERIUM EXCESS

FREQUENCY (n)

FIGURE 12: HISTOGRAM OF DELTA 0-18 OF CANAL MM-5l(O {MAY 1983 - APRIL 1988)

¿lLT/4 0-18 CO 2 F

GO "O LO oli- o

h- o:

<

no

238 I FIG. 16 S Ó8 vs TRITIUM UNITS PLOT OF DEEP WATERS IN MARDAN VALLEY -U H3 H2 H1 -10 -9 -8 -7 -6

FIG. 17 6 0 VERSUS CHLORIDE PLOT OF SHALLOW WATERS IN MARDAN VALLEY, MAY 1983. FIG.18 60 18 VERSUS CHLORIDE PLOT OF DEEP WATERS IN MARDAN VALLEY, MAY 1983. 200

FIGURE 19: COMPARISON OF £M4'fc 0-18 OF 185 SURFACE ÂNd SUBSUBFÂCB WATERS

170 IN ÍÍARDAN YALLEY '

155

140 m m

125

* •- ..

110 *

05

m 80 m

m 50 -12 -11 -10 -8 -8 -7 -6 -5 0-18% - C-íi (pmc)

FIGURE 20: COMPARISON Orq-U AND C-13 0? 185 — ' •» ¡fÜMACEANp'.SVpSURFÂCE WATERS

170 — III ilÂRMN'YÀLLUY

î 155 —

140

125

110 3K 3K

95

m

80 — * m *

65 IK m m .. 50 1 1 III'! II -3 -4 -5 -6 -7 -8 -9 • -10 -11 -12 -13 -14 -15 C-131% #C-I4(jmic)

FIGURE SI: COMPARISON OFC-14 AND ff-3 0F 195 SURFACE AN» SVBSMFACS WATSItS

170 — m WLRDAN VALLEY

155 —

..- 140 _ m m *

125 * *

110 m. m

* .. * 95 m

m

80 m

65 m *m

50 | III III 0 15 30 45 60 75 90 105 12» 135 150