The Lower Jordan River: River Salinization, Relationship with Adjacent Groundwater and Future Management
Thesis submitted in partial fulfillment of the requirements for the degree of “DOCTOR OF PHILOSOPHY”
by
Efrat Farber
Submitted to the Senate of Ben-Gurion University of the Negev
Approved by the advisor ______
Approved by the Dean of the Kreitman School of Advanced Graduate Studies
______
November 2005
Beer-Sheva
This work was carried out under the supervision of
Dr. Avner Vengosh
In the Department of Geological & Environmental Sciences
Faculty of Natural Sciences
Title: The Lower Jordan River: River Salinization, Relationship with Adjacent Groundwater and Future Management
By: Efrat Farber Supervisor: Dr. Avner Vengosh
Abstract: The objective of this study was to investigate the geochemical system of the lower Jordan River and associated groundwater in order to evaluate the origin of river salinization, the relationship with adjacent groundwater, and consequent suitable management activities required to maintain or improve river water quality. The study is comprised of a general introduction, three separate discussion papers, and a general summary. The Introduction (1.1) discusses the global phenomena of river salinization processes, the hydrological and hydrogeological background of the Jordan Valley, and analytical procedures employed during this study. The following chapters present the results from the lower Jordan River and regional groundwater, and implications for groundwater management. Although each can be read independently, with its introduction, results and discussion, the sections in Chapter 2 are arranged such that each one defines a different way of looking at the hydrological system of the lower Jordan River and its vicinity. The first section (2.1) discusses the origin and mechanisms of salinization in the lower Jordan River, and has been published in Geochimica Cosmichimica Acta (Farber et al., 2004). The second (2.2) deals with the geochemistry of groundwater resources in the Jordan Valley and evaluates the impact of the Rift Valley brines. It has been accepted to Applied Geochemistry. The third section (2.3) aims to predict the future salinity variations of the lower Jordan River under several different management scenarios that are included in the peace treaty between Israel and Jordan. It can be found in Applied Geochemistry (Farber et al., 2005). The Summary (Chapter 3) provides a comprehensive framework combining all the conclusions regarding the chemical and isotopic variations along the lower Jordan River, the different sources that control the river water's quality and the impact of those findings for future management of the lower Jordan River.
Preface
The objective of this study was to investigate the geochemical system of the lower Jordan River and associated groundwater in order to evaluate the origin of river salinization, the relationship with adjacent groundwater, and consequent suitable management activities required to maintain or improve river water quality. The study is comprised of a general introduction, three separate discussion papers, and a general summary. The Introduction (1.1) discusses the global phenomena of river salinization processes, the hydrological and hydrogeological background of the Jordan Valley, and analytical procedures employed during this study. The following chapters present the results from the lower Jordan River and regional groundwater, and implications for groundwater management. Although each can be read independently, with its introduction, results and discussion, the sections in Chapter 2 are arranged such that each one defines a different way of looking at the hydrological system of the lower Jordan River and its vicinity. The first section (2.1) discusses the origin and mechanisms of salinization in the lower Jordan River, and has been published in Geochimica Cosmichimica Acta (Farber et al., 2004). The second (2.2) deals with the geochemistry of groundwater resources in the Jordan Valley and evaluates the impact of the Rift Valley brines. It has been accepted to Applied Geochemistry. The third section (2.3) aims to predict the future salinity variations of the lower Jordan River under several different management scenarios that are included in the peace treaty between Israel and Jordan. It can be found in Applied Geochemistry (Farber et al., 2005). The Summary (Chapter 3) provides a comprehensive framework combining all the conclusions regarding the chemical and isotopic variations along the lower Jordan River, the different sources that control the river water's quality and the impact of those findings for future management of the lower Jordan River.
Contents Preface ...... I 1. Introduction...... 1 1.1. River salinization in the world...... 1 1.2. Hydrology and Hydrogeology of the Jordan Valley...... 8 1.3. Methods...... 12 1.3.1.Fieldwork 12 1.3.2.Analytical techniques: major and minor ions……………………………..12 1.3.3.Analytical techniques: 87Sr/86Sr, δ34S, δ11B, δ15N and δ18O Isotopes. 12 1.3.4.Drilling procedure 14 2. Results and Discussion ...... 15 2.1. The origin and mechanisms of salinization of the lower Jordan River ...... 15 2.1.1. Introduction…...………………………...………………………………..15 2.1.2. Results and Discussion 15 2.1.3. Conclusion 36 2.2. The geochemistry of groundwater resources in the Jordan Valley: impact of Rift Valley brines ...... 38 2.2.1. Introduction 38 2.2.2. Results 44 2.2.3. Discussion 56 2.2.4. Summary and conclusion 70 2.3. Management scenarios for the Jordan River salinity crisis...... 71 2.1.1. Introduction 71 2.1.2. Methodology 74 2.1.3. Results and Discussion 76 2.1.4. Conclusions 96 3. Summary...... 99 4. References...... 103 5. Appendix I: analytical results…………..……………………………………….. 110
1. Introduction
1.1. River salinization throughout the world
River salinization is a phenomenon that has shaped human history since at least the fourth millennium BC. New evidence suggests that the rise and collapse of early civilizations (e.g., the Akkadian, 4200 BC) were affected by the salinization of their rivers (e.g., the Tigris and Euphrates rivers; Cullen et al., 2000; deMenocal, 2001). While prehistoric salinization is associated with both climatic changes and man’s activity through irrigation practice, modern salinization is caused primarily by direct and indirect human activities. The water quality of many rivers in arid and semiarid areas is deteriorating due to a combination of extensive land-use changes, diversion and damming of rivers, generation of saline agricultural return flows, and sewage dumping. The results are striking: the rise in salt content causes a decrease in biodiversity, a replacement of the halo-sensitive biota with halo-tolerant species, soil salinization, and diminishing water resources (Williams, 2001). The dominant factor determining the river quality in water-scarce areas is the balance between freshwater withdrawal, groundwater discharge, and agricultural return flow. As more fresh surface water is diverted, the impact of the agricultural return flow increases (Pillsbury, 1981). The rise in the salt content of rivers such as the Colorado and Arkansas rivers in the United States is derived from a combination of upstream diversion of fresh water, intensive irrigation, and formation of saline agricultural return flow, which enters the river (Pillsbury, 1981; Gates et al., 2002). Similarly, saline agricultural drainage increases the salt contents of the Nile (Kotb et al., 2000), Euphrates and Tigris rivers (Robson et al., 1983; Beaumont, 1996). In contrast, the source of the dissolved salts in the Murray River in South Australia (Allison et al., 1990; Herczeg et al., 1993) and the Rio Grande in the United States (Phillips et al., 2003) is geogenetic and derived from the discharge of saline groundwater. Despite the importance of river salinization in dryland environments, only a few studies have investigated the full chemical and isotopic compositions of salinized rivers (e.g., Herczeg et al., 1993; Phillips et al., 2003). The lower Jordan River is located in the semiarid region of the Jordan Valley, along the border between Israel and Jordan. The water discharge and the size of the Jordan
1 River are relatively small, compared to other rivers in the ME, such as the Nile, Euphrates and Tigris Rivers. The Jordan River has historical and religious importance and it serves as a borderline throughout history. Its importance to the neighboring communities rises from these facts not less and perhaps more than its importance as a water resource. The flow rate of this river changed dramatically during the second half of the 20th century. The severe reduction in water flow during the last few decades has resulted in a significant degradation of river water quality. At the southernmost point of the Jordan River, chloride content has increased from 400 mg/L between 1925 and 1947 to ~3000 mg/L at present. Under conditions of low flow rates and poor-quality water, the potential influence of external sources on the river's discharge and chemical composition has become significant.
2 N Lebanon A Syria Sea of Upper
Galilee River Jordan Y ar mo uk a Sea of Galilee iy n 1 Israel a Saline P Carrier it T B 2 Palestinian Alumot W Authority Dam W Jordan 3 Deganiya Lower Jordan River 0
0 E 32 N 4 Dam 0 ! 35 5 Adassiya ! Dead Sea Yavniel Dam Yarmouk ! 6 ! 7 9 !
25 km 10 l a n Naharaim a
510 C
Hydrometric st. a ) 8 l l C a A 11 d ! b K ( b A a H Ar g l- n E i . K W 12 Tavor b ra ! A am 13 14 D
!!
!! 15 KAC 15
Issashar
16
!! W. Teibeh 18 20 19 W. Ziqlab 025 20 17 21 22
Harod !
23 ! Sheich- 24 Legend Nimrod Hussein Br. River Samplingsampling site 25 Tributary Sampling site Groundwater sampling site 18 Site # Bridge Crossingcrossing km Dam/Wier Shif’a 26
3 N Lebanon B25 Orkit Canal Syria Sea of Upper Galilee Jordan River Y ar mo Hisha Canal uk 30 KAC Israel Bezek Palestinian Authority 35 Jordan
W. Yabis River Jordan Lower
0
E 32 N 0 40
27 35 W. El-Maliach Dead Sea
45 28 W. Kufranja
25 km 29 50 30 31 W. Rajib 32 55 33 ( W T 34 . ir F t
60 a c raa ha 35 Zarqa R. ) 36 65 37 38
40 70 39 41 W Adam (Damya) Br. . E 42 l-A 43 h’ 44 75 ma 45 r 46 47 80 (KAC) W. Mallaha
85 W. Melecha
48 AbdallaKing Canal b Uga ei 90 u Sh 49 . W. Nueima W Allenby Br. 95
53 50 51 in W. Kelt fra Legend
100 52 a . K 54 W River Samplingsampling site Tributary Sampling site km Abdalla Br. Groundwater sampling site 18 Site # Dead Sea Bridge Crossingcrossing
Fig. 1. Detailed maps of the northern (A) and southern (B) parts of the lower Jordan River. Sampling points along the river, inflows and shallow boreholes are marked and listed in Table 1.
4 NO3 Br B Sr 3 efers HCO ted ted 4 SO 9.9 4.2 40.7 1.1 61.1 1.7 4.9 100 363 59 94 TDS Ca Mg Na K Cl 4144 water O 18 δ δ δ δ nitrate N 15 δ δ δ δ sulfate S 34 δ δ δ δ Sr 86 Sr/ 87 B 11 δ δ δ δ Date km ‰ ‰ ‰ ‰ mg/l mM mM mM mM mM mM mM µM µM µM µM Distance Distance from Alumot from River Eastern inflows and groundwater groundwater and Inflows Western Initial sources Initial Northern section Northern JR-225 3 Bitaniya 0 22/04/2001 2.2 4.6 1811 1.4 3.7 12.0 2.3 13.4 0.9 12.0 16 30 28 10 Table 1: The chemical and isotopic compositions of representative samples from the Jordan River water, inflows and groundwater inflows water, groundwater and River Jordan the from samples of representative compositions isotopic and chemical The 1: Table repor are constituents of individual content The Sea. Dead and of Galilee Sea the between Valley, Jordan of the vicinity the in in mmole/l, where the overall TDS values are in mg/l. Location of the sampling sites are marked in Figure 1. Distance km) (in r Dam. at Alumot flow to initial River the of Jordan the JR-187JR-368 9JR-359 1 yarmouk Fresh 10 1 yarmouk Fresh 2 yarmouk Fresh 2.6 2.6 3.3 04/12/2001 31.5 01/03/2002 01/03/2002 0.70752 31.8 32.8 0.70754 0.70758 10.6 10.2 11.7 11.4 735 733 779 1.9 1.9 2.0 1.3 1.4 1.5 3.9 4.1 4.2 0.2 0.2 0.2 3.4 3.8 4.1 0.8 0.8 1.0 5.3 4.9 5.0 161 145 189 13 13 13 12 16 11 14 11 14 JR-007JR-92 4JR-91 Bridge Alumot JR-89 8JR-94 Bridge Alumot 12 Bridge Dalhamiya JR-96 Gesher 13JR-004 0.1 - North ur Neve 15JR-84 26 - South ur Neve 5.6 0.1 Station Shifa' 01/09/1999 29.2 11.6 08/08/2000 Station Shifa' JR-005 08/08/2000 12.7 0.70775 31.6JR-67 32.8 11 8.7 08/08/2000 River Yarmuok 0.7077311 28 19.6 0.70779 08/08/2000 34.81A 13.5 08/08/2000 32.3 20.02B 27.7 0.70764 River Yarmuok 10/01/2003 14 33.53A 0.70762 Arab Wadi 6.3 31.5 4.34A 0.70773 08/08/2000 16 4.9 0.70771 Arab Wadi Teibeh 33.8 Wadi 17 11.7 6.3 09/01/1999 Waqqas 0.70770 25 3.8 36.2JR-60 15.5 Ziad Abu -4.2 24/05/2000JR-59 12.2 0.70719 5.9 22 4673 4007JR-58 36.7 -3.3 Harod 16.5 -2.7 23 12.2 -2.1 10.6 19/09/2000 48 0.70716 canal Water 4264 16.1 8.9 24 3760 -3.6 4443 Nimrod Wadi 25.7 04/01/2001 27/02/2001 17.6 9.8 4.9 23.4 0.70784 7.4 21.0 -2.4 4.5 4443 8.4 18.7 0.70790 47.8 21.4 27/02/2001 0.70775 4.4 3761 38.5 27/02/2001 9.1 6.0 1.6 29.8 6.9 3523 22.2 1.2 -5.4 20.8 28.8 -3.9 43.0 24/05/2000 6.2 0.70793 68.4 34.4 5.2 42.6 57.5 0.70870 4.9 1.2 38.2 24/05/2000 1.1 1.8 24/05/2000 1.2 2.3 7.0 0.70792 3245 62.4 42.2 38.0 39.5 -3.3 48.0 5.6 59.0 7.5 1.3 5.3 1.8 0.70791 35.2 0.70782 3.6 3.9 3371 4.9 16 64.9 33.5 0.9 5.1 32 6.3 0.9 5.2 2.8 3.6 313 8.1 47.1 338 16 194 44.3 55 113 5.4 3.9 27.4 55 3583 678 375 1599 8.5 275 4.3 99 325 0.8 7.0 113 78 45 74 7.6 5.5 83 1.6 30.5 3.3 29.4 350 161 89 -4.6 62 0.7 75 177 7.5 65 1074 10.0 200 1.5 3.8 -3.8 406 31.9 4864 -2.9 143 83 7.4 65 18.4 1.8 7.4 11.4 3903 4.2 65 3914 7.2 1.4 1.4 49 258 1.2 7.1 40 0.2 4.7 15.6 6.4 106 5.4 10.1 1.9 8.5 16.5 161 4.9 176 8.7 47.8 9.7 125 5.3 6.2 24 6.1 3.2 1.1 0.2 0.7 205 35.0 677 0.2 39.4 3.2 68.4 24 6.9 0.5 0.7 33 3.3 110 3.4 4.2 4097 54.4 55.3 120 1.0 7.0 8 13 106 2.5 2.1 113 20 6.0 7.3 548 213 10 613 13 32 73 46 13 163 100 55 48 5 28 40 27 43 13 28 11 ID Loc. Name JR-008JR-107 1 Galilee of Sea 2 Carrier Saline 0.0 0.0 01/09/1999 25/09/2000 25.5 32.0 0.70749 0.70774 11.6 -4.4 662 1.1 1.4 6.0 0.2 7.3 0.6 2.0 5 23 12 8 5 NO3 Br B Sr 3 HCO 4 SO mg/l mM mM mM mM mM mM mM µM µM µM µM TDS Ca Mg Na K Cl water ‰ O 18 δ δ δ δ nitrate N 15 δ δ δ δ sulfate S 34 Table 1. 1. (Continued) Table δ δ δ δ Sr 86 Sr/ 87 B 11 ‰‰‰ δ δ δ δ Date km Distance Distance from Alumot from Fish Pools Fish River groundwater and inflows Eastern Western Inflows and groundwater section Southern River Drainage ID Loc.JR-61 section Central JR-73 18JR-72Well - Hamadia 20JR-55 Huga En 21JR-189 Spring Hasida JR-197 5 18.2JR-354 Spring A-tin b Degania 6 - GW afikim 7 24/05/2000 20.9 h1 Kochvani 20.4 31.7 24/05/2000 0.70741 31.8 24/05/2000 41.2 1.0 2.2 43.2 0.70780 24/05/2000 2.2 0.70783 34.2 04/12/2001 04/12/2001 01/03/2002 0.70794 26.5 22.7 27.1 0.70755 0.70760 0.70754 -1.4 3650 -3.3 -3.0 5.0 7.3 3349 3241 -1.8 8.0 6.3 6.1 3845 33.2 6.9 5.5 0.8 6.2 4027 1632 3251 29.7 42.3 11.1 28.8 9.1 0.7 2.3 4.5 5.7 0.5 32.5 46.1 6.5 44.0 0.5 8.5 2.8 8.1 2.2 2.4 53.3 8 27.0 14.3 25.0 5.6 2.8 5.6 1.4 0.9 1.6 200 371 6.8 32.4 18.2 355 23.1 80 138 10.5 113 1.7 9.2 42 48 32 8.0 31 4.8 7.2 175 31 2065 32 49 1323 16 128 103 54 148 38 167 26 24 33 13 JR-86 19JR-50Eden - Hamadia 28 Gibton10 20.789 08/08/2000 297 Seebiya Rajib 31.512 30 0.70762 Bassat Faleh13 31 44 -Botton Faleh 14 32 33 Bweib Mikman Wadi 49 34 24/05/2000 Hawwaya 35 36.71JR-014 Mifshel 51 19/09/2000 51 0.70785JR-51 27 26.97 maliach el Wadi JR-247 55 18/09/2000 0.70804 18/09/2000 30.22 53 maliach el Wadi 40.46 0.4 57 18/09/2000 maliach el Wadi 0.70806JR-81 0.70809 38 26.22JR-103 4436 59 18/09/2000 36 0.70804JR-80 18/09/2000 Station Zarzir 29.22 38 09/11/1999 6.6JR-102 19.73 38 0.70797 38 Station 18/09/2000 Zarzir JR-233 0.70820 Bridge Adam -3.3 28.97 23/05/2000JR-100 8.3 06/04/2001 Bridge 0.70827 Adam JR-126 37.96 44 59.7 2983 Bridge Adam 42.6 Station Tovlan JR-231 0.70776 59.7 1.4 3.4 66.4 08/07/2000 Station Tovlan 57.3 1862 32.6 Station Tovlan 66.4 25/09/2000 7.1 08/07/2000 6.4 22.2 72.4 66.4 0.70797 32.5 3.2 1883 30.7 2982 25/09/2000 4.3 28.6 0.70788 72.4 6.3 25/09/2000 23/04/2001 0.70810 30.5 3847 0.7 3.1 5.1 72.4 6.3 161 30.0 0.70806 27/02/2001 38.4 7.2 300 7.2 1962 13.3 16.4 0.70805 23/04/2001 5900 4.9 -4.6 32.0 7.6 111 3.9 0.6 -4.1 4.1 0.70804 10.5 64 15.4 16.7 5038 -2.2 3033 12.6 13.7 19.9 16.8 4.1 3123 0.6 23.8 1.0 3.1 3458 5.1 8.7 14.9 6.2 48 -3.2 14.3 -2.2 1.5 6.4 10.4 30.6 5.1 14.4 25.5 12.6 4.2 114 23.2 13.9 3617 4.6 5.2 4.8 3459 4.1 1160 -2.1 0.7 4.4 14.0 76 30.3 -1.7 6.7 6.1 102 4.5 7.9 29.7 27.5 5.1 10.4 3199 3409 6.1 35 4.4 29.4 119 0.9 26.8 2280 3881 700 6.2 32.6 1.1 2440 79 28.1 6.9 7.9 5.3 7.5 7.1 37.7 54 267 -3.7 1.2 4.7 5.8 64 42.3 22.3 34.4 3.5 1790 71 31.5 76 41.5 5.3 3902 167 1640 7.4 3.7 3.5 1.4 38 1.0 28 4.7 8.2 112 29 5.4 64 2000 3.0 28.9 31.8 6.1 42.3 246 41.6 323 4.7 35.2 1.0 70 24 1.1 161 -3.1 6.1 121 4782 4.6 1.3 188 8.4 25 39.4 177 41.2 77 232 4.7 5970 6.0 81 45.7 7.0 150 3.8 5.2 18 35.1 65 226 59 6.2 295 8.4 92 1.3 5.0 4.1 65 10.9 138 135 0.4 46 43.1 281 13.0 102 332 43.5 74 6.5 365 51 163 1.7 131 54.4 46 150 0.6 56 54.0 79 2.0 111 60 51 8.3 71.2 565 56 10.5 200 6.9 106 0.4 394 68 415 212 365 129 176 68 80 6 NO3 Br B Sr 3 HCO 4 SO mg/l mM mM mM mM mM mM mM µM µM µM µM TDS Ca Mg Na K Cl water O 18 δ δ δ δ nitrate N 15 δ δ δ δ sulfate S 34 Table 1. (Continued) 1. Table δ δ δ δ Sr 86 Sr/ 87 B 11 ‰‰‰‰ δ δ δ δ Date km Distance Distance from Alumot from Southern section Eastern inflows and groundwater groundwater and Inflows Western River (continued) IDJR-45 Loc. JR-78 47JR-230 107 - Gilgal JR-002 107JR-76 - Gilgal 49 107 - Gilgal Bridge Allenby JR-332JR-001 76.6 BridgeJR-75 Allenby 50 Bridge Allenby site Baptism JR-331 91.4 76.6 23/05/2000JR-74 76.6JR-99 site 33.0 Baptism 09/01/1999 91.4 54 site 08/07/2000 Baptism JR-330 91.4 Bridge 0.70814 23/04/2001 Abdalla 30.7 95.6 08/07/2000 0.70820 Bridge Abdalla 08/12/2001 Bridge Abdalla 31.76 09/01/1999 95.6 100.0 5.8 0.70807 95.618A 31.017B 14.5 100.0 08/07/2000 08/07/2000 0.70813 5.0 100.0 08/12/20014 37 31.6 River Zarqa 25/09/20005 5.7 -2.8 7.1 0.70816 08/12/2001 River Zarqa 16.224A 30.2 River Zarqa 540616B 40 0.70805 6.4 15.75 Rasif -2.415 41 42 6.4 Mayyala Abu Aqraa25A 66.3 -1.9 4724 16.82 4851 66.3 12.3 Aqraa 431 4350 7.3 45 66.3 Gdeida 5.6 18/09/2000 Mallah 5.6 Mallaha -4.7 51.1 27/02/2001 14.8 24.7 -3.4 5.2 70.3 51 1.9 04/01/2001 17.13 24.2 10.4 5063 0.70871 Kharar 10.6 4886 52 69.2 6120JR-48 27.5 65.1 0.70868 -1.6 -2.9 Kafrain Hisban 48.7 18/09/2000 9.3 70.4 70.3 46.1 5.9 -2.9JR-46 0.70857 10.1 5.6 2.0 39 28.7 8.6 4469 7866 2.0 9.5JR-43 18/09/2000 Upper 40.7 Tirtcha 4.6 70.3 6218 46 18/09/2000 0.70822 27/02/2001 55.8 11.3JR-77 10 72.5 33.7 57.5Ah'mar 10.7 el Wadi 1.6 6.5 48 9.2 13.8 28.5 98.8JR-333 48.2 371 8.1 -2.3 7.0 Melecha Uga 0.70836 47.8 9.4 04/01/2001 52.8 45.7JR-13 0.70807 56.1 0.70802 27/02/2001 263 96.8 2.1 4.1 17.7 10278 9.6 48.6 2.0 -2.4 13/09/2000JR-52 7.7 4.0 Melecha Uga 66.7 2.0 14.6 29.5 176 Melecha Uga 75.0 62.1JR-41 12.5 0.70794 40.2 73.9 58.8 274 11095 40.7 4.4 79 13/09/2000 0.70810 75.0 484 57.9 Spring Sukot 9.1 3.4 23/05/2000 0.70816 86.7 288 9.4 1.5 53 10.2 29.0 10.2 13.6 23/05/2000 24.4 185 2.6 Spring 306 Sukot - Well Hagla 5.6 40.2 97.8 166 4.1 54.4 0.70805 41.7 176 4.0 6.3 86.7 79.0 250 97.9 23/05/2000 29.0 0.70800 15.2 4518 86.7 4245 71 274 7.2 0.70796 10.8 139 4.2 477 397 41.7 100.0 4796 3.9 37.4 08/07/2000 363 6.0 59 8.8 131.8 4.2 5.2 4.3 202 308 0.70797 08/12/2001 4.3 37.4 18.3 176 403 96.7 6.3 166 171 151.5 41.5 11360 306 379 29/03/2000 74 8.6 4.0 9.0 563 17.2 73 82 0.70804 23/05/2000 401 253 47.5 8.2 23/05/2000 12450 8.5 231 4.2 45.7 484 30.8 213 71034 129 3811 -16.7 108 43.5 68497 11.3 2.6 1.7 826 46.5 90 67 333 12.7 59.2 15508 0.70799 7.7 49.2 2.7 268 1014 48.2 38.3 -3.0 30.8 137.0 0.70798 18.5 -4.3 188.8 153 259 12.0 3.9 -17.1 48.5 11.6 185.1 118.7 10.3 62911 159 726.4 7386 122.9 3.4 739.5 11.9 25.0 0.0 5.8 27.0 5741 -4.7 88.1 11.11 29.4 22.0 26.0 1170.6 136.4 4.8 167.5 1078.3 1010 8.5 790 43.6 11.8 11.3 2.6 31.6 5274 6.4 43.1 7.8 163.6 131 -6.2 116 0.0 16 4.54 27.2 5.1 601.2 166.4 4.4 2040 19.5 210 7.5 9.8 9.2 235 29.0 5391 13.5 40.9 5251 1355 113 675 1810 88 1069.0 8065 94 54.7 6821 -4.8 47.4 48.6 6.1 18.8 1098 0.0 191 -5.0 691 9262 7.6 13.5 1908 7.5 2.2 1916 748 4.0 170 3.4 96 516 -4.8 1.8 1632 2225 491 2333 90 42.8 146 75.5 14.4 65.9 62.2 451 14.1 1648 2.3 3.7 14.0 2 98 1227 5.9 8.6 9.2 43.5 44.6 171 19.2 63.5 1069 3.7 7885 2.6 10.0 11.3 2.6 161 3.6 9.7 430 258 7.2 65.9 990 220 63.5 793 3.7 300 5.4 10.4 12.5 9.6 322 230 9.3 217 0.1 1.3 10.0 500 147 106 76 5.2 5.1 12.1 0.1 236 26.8 388 113 403 1.8 484 12.6 231 3.5 451 66 1.9 7.4 44 4.1 185 241 1613 7.4 65 661 66 38 1619 63 36 31 63 13 25 110 14 7 1.2. Hydrology and hydrogeology of the Jordan Valley The total length of the Jordan River, from its origins in the Hermon mountains in the north to its mouth at the Dead Sea, is approximately 250 km (aerial distance), but its meandering course increases its length to 330 km (TAHAL, 2000). The river is located in a semiarid area and can be divided into two sections: the upper Jordan River, from the Hermon Mountains to the Sea of Galilee (Lake Tiberias), and the lower Jordan River, from the Sea of Galilee to the Dead Sea. The latter section also marks most of the border between Israel, the West Bank and the Kingdom of Jordan (Fig. 1). Whereas the upper Jordan River is a major source of high-quality drinking water, the water discharged from the Sea of Galilee into the lower Jordan River has been historically more saline and therefore of lower quality (Nissenbaum, 1969). The construction of two dams at the outlet of the Sea of Galilee has resulted in further deterioration of water quality and quantity in the lower Jordan River. Currently, there is no input of water from the Sea of Galilee to the lower Jordan River. Water quantity has decreased from a historical volumetric discharge estimated at around 1300 MCM/year (Salameh and Naser, 1999) to a recently measured and estimated base flow of 30 to 200 MCM/year (Holtzman et al., 2005; TAHAL, 2000, respectively), with rare high-discharge (~600 m3/s) flood events. Holtzman et al. (2005) measured the discharge under draught conditions (i.e., only base flow) while TAHAL (2000) estimated the discharge including floods, which occur mostly during very rainy winters, when the dams at the Sea of Galilee and/or at the Yarmouk River are opened. Historical contributors included the outlet from the Sea of Galilee (540 MCM/year), the Yarmouk River (480 MCM/year), local streams, and floods (Hof, 1998). Following the construction of water projects in Israel, the Kingdom of Jordan and Syria, both the Sea of Galilee and the Yarmouk River have been dammed and no fresh surface water flows into the lower Jordan River, other than negligible contributions to the river’s base flow and the aforementioned flood events. To reduce the salt contents of the Sea of Galilee, natural saline springs in its vicinity (e.g., Tiberias Hot Springs) are diverted through the "saline water carrier" to the lower Jordan River (15 to 20 MCM/year). Together with sewage effluents (~10 MCM/year), the saline water carrier currently forms the primary water source (the base flow) of the lower Jordan River, while the Deganiya and Alumot dams at the outlet of the Sea of Galilee prevent the entrance of fresh water from the Sea of Galilee (~250 mg Cl/L). Alumot Dam, which is located downstream of Deganiya Dam, represents, for the
8 purposes of this study, the beginning of the lower Jordan River. In fact, all of the water samples in this study were taken from Alumot Dam in the north (the “zero point”) to Abdalla Bridge (100 km aerial distance downstream of Alumot Dam).
The discharge of the Yarmouk River (Fig. 1) to the lower Jordan River has been drastically reduced due to upstream water use in Syria and the building of the Adassiya Dam on the Yarmouk River for water diverted between Israel and the Kingdom of Jordan (Klein, 1998). Accordingly, the current contribution from the fresh Yarmouk to the lower Jordan River is nearly zero and the water downstream of the Adassiya Dam that enters the lower Jordan River is saline. Other water sources that flow into the lower Jordan River include drainage from fishponds, wastewater, fresh and saline springs, and agricultural return flows. At present, only 30 to 200 MCM/year (Holtzman et al., 2005; TAHAL, 2000) of mostly poor-quality fluids reach the Dead Sea through the lower Jordan River. This dramatic reduction in water flow during the last few decades has resulted in a significant deterioration in river water quality (Hof, 1998; Klein, 1998). Archival data (from Bentor, 1961; Neev and Emery, 1967) reveal that at Abdalla Bridge, at the southernmost point of the Jordan River, chloride contents were ~11 mM between 1925 and 1947 but have increased to >85 mM at present. The most prominent outcome of the dramatic reduction in the discharge of the Jordan River, which is the main water source for the Dead Sea, is the >20 m decline in the Dead Sea water level over the last few decades (Yechieli et al., 1998).
The Jordan Valley is a pull-apart basin, with a width of 5 to 9 km in the north and up to 23 km in the south. Its eastern and western boundaries are the escarpment caused by the faults of the Syrian-African Rift Valley. The valley drains groundwater that flows from adjacent basins (Fig. 2). In the northern part of the lower Jordan River (0- 20 km downstream from Alumot Dam), groundwater flows primarily from basaltic aquifers, one on the western side (Tiberias Group; Möller et al., 2003), and one on the eastern side that is part of the Yarmouk basin (Fig. 2). In addition to basaltic aquifers, on the western side of the Jordan Valley, groundwater also flows from calcareous aquifers (Judea, Mt. Scopus and Avdat groups). On the eastern side, three major aquifer systems are identified: (1) the Amman-Wadi Sir (Ks) aquifer (Upper Cretaceous to Paleocene limestone and chert of the Belqa Group); (2) the Hummer
9 (Kj) aquifer (Upper Cretaceous dolomitic limestone of the Ajlun Group); and (3) the Kurnub (Kk, Lower Cretaceous) and Zarqa (Ja, Jurassic) aquifers (Salameh, 1996; EXACT, 1998). The lower Jordan River is incised into Pleistocene sediments that fill the Jordan Valley. In the northern section, the sediments are composed of marl, sand, conglomerate, calcite, and diatomite (Hazan, 2003). In the southern part, the sediments are composed of the Late Pleistocene Lisan Formation (alteration of aragonite, marls, detrital and gypsum layers) overlying the Neogene-Pleistocene Samra Formation (alternation of marl, sand, conglomerate, oolitic limestone, chalk; Begin et al., 1974; Landmann et al., 2002; Waldmann, 2002). Along the entrances of side wadis into the Jordan Valley, the lithological composition is altered by alluvial and detrital sediments (e.g., sand, conglomerate). The relatively high conductivity of the detrital sediments results in the formation of local aquifers (e.g., Jericho area; Gropius and Klingbeil, 1999; Marie and Vengosh, 2001). In the northern part, the association of basaltic rocks along both sides of the valley (Fig. 2) resulted in the formation of basalt gravels within the Jordan Valley (as found in the northern borehole which was drilled during this research). In the central and southern parts, the composition of the alluvial materials mimics those of the rocks along both sides of the valley. The morphological structure of the Jordan Valley is composed of the present flood plain of the lower Jordan River (the "Zor") and past flood plains at higher elevations (the "Ghor"). In most cases, the modern lower Jordan River and thus the "Zor" area is incised in the underlying Samra Formation whereas the upper Ghor plain is composed of the Lisan Formation (Fig. 2D), and in some cases also the Holocene Zeelim (Damia) Formation (Landmann et al., 2002).
10 NW SE B JORDAN 400 Bira 2 VALLEY 0 m, MSL
JUDEA GR. -400 -800
-1000 5 km JUDEA GR. A A’
A TIBERIAS GR. – Basalts (Upper & Lower)
Sea of Galilee TIBERIAS GR. – Marl & Clay
AVDAT GR. - Limestones Upper Upper River Jordan
Mt. SCOPUS GR. – Chalk & Marl Yarmouk River JUDEA GR. – Dolomites & Limestones Yarmouk Basin GROUNDWATER FLOW River Lower Jordan Northeastern Northeastern Basin
Side C
Eastern Eastern Basin Mountain Wadis Basin W E Western Escarpment of the Jordan Valley Floor Eastern Escarpment of the Jordan Rift Valley Jordan River Jordan Rift Valley Ks 600m Jordan KjKj Kk p Kk Valley Alluvium rou . Sea level Judea Gr upp. JaJa Ju Gderou uun rrou a Gpr Kj Q Ajljl b G Floor oup K Q11 A nub p Dead Sea Dead j ur oup (-600)m Ku Gro Dead Sea Dead Kur JordanJordan ValleyValley Group rqa Basin nub G Zarq Ku roup Q Z rnub G Kk Group2 (-1200)m roup K Rift k Q 2 (-1800)m Ara Valley Arad GdrGro oupu Jpa Ja Faults Not to scale 25 km
W E “Ghor” The Jordan River Lisan Fm.
50 m “Zor” Samra Fm.
Fig. 2. A. Groundwater basins and groundwater flow direction (indicated by arrows) in the Jordan Valley. B. Schematic geological cross section of the northern Jordan Valley (from Moller et al., 2003); C. Schematic hydrogeological cross section of the southern Jordan Valley (after EXACT, 1998); D. A shallow morphological structure at the Abdalla Bridge site.
11 1.3. Methods
More than 100 sites were selected in the Jordan Valley, including river water, springs, boreholes, streams, drainage ponds and fishponds on both sides of the lower Jordan River, between the Sea of Galilee and the Dead Sea (Fig. 1). The sites were sampled throughout the hydrological year to monitor seasonal variations. Overall, 650 water samples were collected during ca. 20 field trips from September 1999 to June 2005.
1.3.1. Fieldwork (sampling procedure and field measurements) Electrical conductivity, water temperature, pH, turbidity, and dissolved oxygen were measured in the field (using HORIBA water-quality checker U-10). Water samples were collected in new plastic bottles that were rinsed several times with the sample waters before storage. Samples were collected in separate bottles for chemical, solute isotope (B, Sr, S, N), and oxygen isotope analyses, respectively. Samples that were analyzed for solute content and isotopes were filtered (0.45µm) within 24 to 48 h after sampling. After sampling, the samples were stored at 4°C, until analyses were performed.
1.3.2. Analytical techniques: major and minor ions The samples were analyzed for major and minor ions (all samples) at the Geological Survey of Israel. Cation and boron concentrations were measured by inductively coupled plasma-atomic emission spectrometry (ICP-AES), anion concentrations by ion chromatography (IC), and bicarbonate by titration. The imbalance between positively and negatively charged ions did not exceed 5%, reflecting the overall precision of the analytical procedures.
1.3.3. Analytical techniques: 87Sr/86Sr, δ34S, δ11B, δ15N and δ18O isotopes
Isotopic ratios of strontium (n = 77), boron (n = 97), sulfur in sulfate (n = 31), oxygen in water (n = 164), and nitrogen in nitrate (n = 18) were determined by different analytical procedures and laboratories as outlined below. Strontium was separated from the water by ion exchange using Biorad AG50X8 resin at Ben-Gurion University. Strontium isotopic ratios were determined by thermal ionization mass spectrometry at the US Geological Survey, Menlo Park, CA, USA. An external precision of 2×10-5 for the Sr isotope measurements was determined by replicate
12 analyses of the N.I.S.T. 987 Sr metal standard. Laboratory preparation and mass spectrometry procedures were identical to those described in Bullen et al. (1996). Boron isotopic ratios were measured by negative thermal ionization mass spectrometry (direct loading procedure; Vengosh et al., 1991a) at the US Geological Survey in Menlo Park. For each water sample, an aliquot containing approximately 2 ng of boron was evaporated on a rhenium filament. For mass spectrometry, all samples were ionized at 950 to 1000oC, and each sample was analyzed in duplicate. The measured 11B/10B ratios were normalized to the N.I.S.T. 951 boric acid standard. At the Menlo Park laboratory, δ11B of seawater is +39.2 ‰ relative to this standard. External analytical reproducibility of boron isotope ratios was 1‰, based on replicate analyses of the N.I.S.T. 951 and seawater standards, and duplicate measurements of 34 individual samples. For δ S analyses, SO2 gas was produced and collected on a vacuum line at the Geological Survey of Israel, following the procedure described by
Coleman and Moore (1978; Gavrieli et al., 2001). Isotopic measurements of the SO2 gas were performed at the British Geological Survey, Keyworth, UK. The δ34S values are reported in per mil relative to the CDT standard. Reproducibility of gas preparation and isotope measurements for an internal laboratory standard was ±0.2‰ over a time period of 5 years (n = 140). NBS-127 δ34S (= 20.3 ± 0.2‰; n = 7) was used to calibrate the internal standard. δ18O values of water were determined using the triple collector VG SIRA-II mass spectrometer at the Geological Survey of Israel. Nitrogen isotope ratios of dissolved nitrate in the water were measured by Michal Segal from the Technion, Israel (Segal-Rozenhaimer et al., 2004) in a parallel study. 2- For these latter measurements, SO4 was removed by precipitation as BaSO4 and - HCO3 by adjusting the pH to less than 4. Nitrate was separated using the ion- exchange resin technique described by Silva et al. (2000). Subsequently, nitrate was converted to AgNO3 at the University of Calgary (Alberta, Canada). Nitrogen isotope ratios were determined on N2 after thermal decomposition of AgNO3 in an elemental analyzer and subsequent continuous-flow isotope ratio mass spectrometry. δ15N values for all samples were calibrated against international reference materials (IAEA N1 and N2). The overall reproducibility of nitrate extraction, gas preparation, and mass spectrometric measurements was better than ±0.5 ‰ based on replicate analyses (n = 10) of saline water samples. The δ18O values are reported in per mil relative to SMOW (Craig, 1961). The analytical precision was 0.01‰, and the external
13 reproducibility of three to four replicates of standards in each run was better than 0.1‰.
1.3.4. Drilling procedure Seven boreholes were drilled in 2003, in the northern part of the research area (10-20 km downstream of the Alumot Dam). In 2004, an additional eight boreholes were drilled in the southern part of the research area (72-77 km downstream of the Alumot Dam). In the northern area, drilling was done with a 50-cm diameter drill bore to a depth of 5 to 9 m (depending on water table level). The piezometers are made of 5-cm diameter, 5-mm thick PVC pipe is perforated at the lowest 3 m of the permeable units (i.e., sand and conglomerate). A gravel pack, consisting of washed quartz gravel, 4-9 mm in diameter, was poured between the tube and the borehole walls. In the southern borehole area, drilling was conducted using a 15-cm diameter drill reaching a depth of 9 to 20 m. The piezometers are made of 7.6-cm diameter, 5-mm thick PVC pipe, perforated in the lowest 3 m. A gravel pack, consisting of washed quartz sand 0.05-2 mm in diameter, was poured between the pipe and the borehole walls. Water was pumped to the surface using a 40 mm pump (Waterra, WSP-12V-2) and the water collected in new plastic bottles that were rinsed several times with the sample waters before storage.
14 2. Results and Discussion
2.1. The origin and mechanisms of salinization of the lower Jordan River
2.1.1. Introduction In this section, we examine the water quality of the lower Jordan River and its tributaries (Fig. 1) between the Sea of Galilee (Lake Tiberias, Lake Kinneret) and the Dead Sea. The chemical composition, and water isotope (oxygen) and solute isotope (strontium, boron, sulfur, nitrogen) compositions of the river, inflows, and groundwater samples were determined in order to evaluate the sources and the mechanisms of inflow of solutes dissolved in the river. Integration of chemical and isotopic tracers with solute mass-balance calculations can serve to delineate the different salt sources and to quantify their impact on the water quality of the lower Jordan River.
2.1.2. Results and discussion Three river sections were identified in terms of salt-content variation along the lower Jordan River (Fig. 3): an upper (northern) section, where the initial high salt content decreases downstream; a middle section, where the variation in dissolved salt content is less significant, and a lower (southern) section, where salt content increases downstream. Together with the salt-content changes, chemical and isotopic variations along the river flow could be observed (Fig. 3). Hypothetically, at least three processes can account for the changing chemical and isotopic compositions of the river water: (1) net evapotranspiration, which would increase the content of conservative solutes downstream. If this were the only process, the ionic ratios and isotopic compositions of conservative constituents in the downstream river segments would be identical to those in the upstream river; (2) inflows from tributaries (point sources) that modify the river-water composition in a step-like function. In this case, the river-water composition would be modified in accordance to the relative contribution of the inflows; (3) groundwater discharge (i.e., a non-point source), in which the river-water composition is gradually modified along the flow due to
15 increasing fractions of the groundwater component. The composition of conservative constituents in the downstream river would reflect the relative contribution of the inflowing groundwater. These hypotheses were examined in light of the water-quality changes observed along the three sections of the lower Jordan River.
Upper Section Middle Section Lower Section 80 May 2000 70 60 August 2000
Cl (mM) 50 40 A February 2001 020406080100 0.7082 B 0.7081 May 2000 Sr 0.7080 86 August 2000 0.7079 Sr/ 0.7078 87 0.7077 0 20406080100 25 C
(‰) 20 15 August 2000 sulfate 10 S
34 5 δ δ δ δ September 1999 0 20406080100 -1.5 D -2.0 August 2000
(‰) -2.5 -3.0 -3.5 water
O -4.0 May 2000
18 -4.5 δ δ δ δ -5.0 0 20406080100 Distance from Alumot Dam (km)
Fig. 3. Chloride concentration, and strontium, sulfur, and oxygen isotopic variation transects along the lower Jordan River. Distance (in km) refers to the beginning of the river flow from Alumot Dam. See Table 1 for the complete isotopic data.
16 2.1.2.1. Chemical modification in the northern section
The initial base flow (~30 MCM/year) of the lower Jordan River (Alumot Dam, Table 2 and Fig. 1) comprises a mix of diverted saline spring water, referred to as the "saline water carrier" (chloride range of 56-78 mM), wastewater from the city of Tiberias, and poorly treated sewage effluents (chloride range of 7-13 mM). A mixture of these source waters is dumped into the river. Based on solute mass balance (Table 3), it was found that the initial flow consists of 60 to 90% of the saline water carrier. The chemical and isotopic compositions of the base flow of the lower Jordan River water 34 (e.g., Na/Cl ~0.65, SO4/Cl ~0.03; δ Ssulfate = 20‰; Table 2) retain the Ca-chloride
(i.e., Ca/(HCO3+SO4) >1) fingerprint of the saline springs that emerge at the western shore of the Sea of Galilee (Starinsky, 1974; Kolodny et al., 1999) and are diverted through the saline water carrier to the lower Jordan River. The initial chemical and isotopic compositions of the lower Jordan River water downstream of Alumot Dam were significantly modified downstream, particularly along the upper 12 km (Figs. 3 and 4). A decrease in Cl-, Br-, Na+, K+, Ca2+, Sr2+ and 34 87 86 2+ 2- 3+ 15 δ Ssulfate, and in the Sr/ Sr ratio, and an increase in Mg , SO4 , B , δ Nnitrate and 18 34 δ Owater values were observed (Table 2 and Figs. 4, 5 and 6). The δ Ssulfate values decreased from 20‰ to 5‰, 87Sr/86Sr ratios decreased from 0.70779 to 0.70760, 18 δ Owater increased from ~-4.5‰ to -2‰, and boron isotopes showed no systematic variation (δ11B between 29 and 35‰, Figs. 6 and 7) despite a significant increase in boron content (Table 2). Overall, the Ca-chloride composition (i.e., Ca/(SO4+HCO3) > 1) of the initial saline water was modified to a Mg-chloride water type and the
Na/Cl and SO4/Cl ratios increased downstream. Figure 5 shows that the contents of different ions tend to correlate linearly with chloride along the river flow. These relationships indicate that the chemical modification of the lower Jordan River water is controlled mainly by mixing of the initial river water with a second water type that has a distinct chemical composition (i.e., Fig. 6). This water source also has low δ34S 87 86 15 18 and Sr/ Sr values and high δ Nnitrate and δ Owater values relative to the initial river water downstream of the Alumot Dam. Table 4 summarizes and Figure 6 illustrates the geochemical characteristics of the known tributaries and groundwater in the upper part of the lower Jordan River: the eastern tributaries (from Jordan), the western tributaries (from Israel), the saline Yarmouk River, and shallow drainage waters that were collected from shallow
17 boreholes around the Yarmouk River (Fig. 1). The chemical and isotopic compositions of the eastern and western tributaries could not account for the observations within the river (Table 4). For example, the western inflows have higher 87 86 Sr/ Sr and lower SO4/Cl ratios than the river water and are therefore not consistent with the trend observed in the river (Fig. 6). In addition, the eastern inflow has a high 87Sr/86Sr ratio. In contrast, the chemical and isotopic variations recorded in the lower Jordan River were similar to those of the saline Yarmouk River and its shallow drainage waters 34 87 /86 (e.g., high Na/Cl and SO4/Cl, and low δ Ssulfate and Sr Sr values, Figs. 6 and 7). Most of the fresh water of the Yarmouk River (TDS ~730 mg/L; Table 2) is diverted to King Abdalla Canal, about 8 km upstream of its confluence with the lower Jordan River. However, the Yarmouk River water downstream of the diversion is saline (TDS ~ 2800 to 8600 mg/L), with distinct chemical and isotopic composition (Table 87 86 2). This composition (Na/Cl = 0.78 to 0.96; SO4/Cl = 0.2 to 0.3; Sr/ Sr ~ 0.70717; 34 δ Ssulfate = −2.1‰) is identical to that of a postulated end member that controls the chemical and isotopic changes observed in the northern section of the lower Jordan River (Table 4 and Figs. 6 and 7). Hence a common groundwater source controls the water quality of both the northern lower Jordan River and the saline Yarmouk River. Since the chemical and isotopic modifications in the lower Jordan River water along the upper 12 km are gradual (Figs. 3, 4 and 5), and are not restricted to the area below the confluence of the saline Yarmouk River 6 km downstream (Fig. 1), we propose that diffuse groundwater discharge is particularly effective along this section of the river. In fact, the water of the saline Yarmouk River is pumped out for fishpond recharge before the confluence with the lower Jordan River and hence its direct contribution is negligible. In addition to the gradual changes, the concentrations of most ions in the lower Jordan River decrease sharply after the confluence of Wadi Arab, ~12 km downstream of Alumot Dam (Fig. 4). However, the water composition of Wadi Arab cannot explain the chemical and isotopic variations of the lower Jordan River water at this point (e.g., the relatively high 87Sr/86Sr ratios of 0.70775 to 0.70784; Table 2). It can be argued that the relatively high inflow of Wadi Arab (Holtzman, 2003), which is characterized by low dissolved-solid contents (chloride range of 4.8 to 8.8 mM; Table 2), causes a point dilution of the downstream lower Jordan River water. Nevertheless, the overall chemical modification of the lower Jordan River is dominated by the groundwater
18 discharge with a significantly lower 87Sr/86Sr ratio. In sum, the results confirm hypothesis #3 that both the Yarmouk and lower Jordan rivers are influenced by discharge of a common (non-point) groundwater source. From 12 km downstream, the groundwater discharge is superimposed with a point surface inflow of Wadi Arab (i.e., hypothesis #2).
Table 2. Major water resources in the vicinity of the Jordan Valley that flow or are associated to the lower Jordan River. Water Source Geochemistry Sample # TDS (Table 1) (g/L)
Initial River Saline springs that emerge at 4.1 to 5.2 Ca-chloride type with low Na/Cl and 2 the western shore of the Sea of SO4/Cl ratios Galilee composed of the “Saline Carrier”
Bitaniya sewage effluents 1.7 to 1.8 High Na/Cl; low SO4/Cl 3 Northern Section Agricultural return flows mixed 1.4 to 8.6 Mg-chloride type enriched in sulfate with 5; 6; 7; 11; 18 with natural saline groundwater high Na/Cl and SO4/Cl ratios; high nitrates Eastern inflow and 0.6 to 3.7 Na-chloride type extremely enriched in 14; 16; 17; 25 groundwater sulfate with high Na/Cl and SO4/Cl ratios Saline western inflows and 3.2 to 4.9 Ca-chloride type with low Na/Cl and 20; 21; 22; groundwater SO4/Cl 23; 24
Central Section Eastern agricultural return 0.5 to 5.9 Mg-chloride type extremely enriched in 29;30; 31; 32; flows sulfate with high Na/Cl and SO4/Cl ratios 33; 34; 35
Western saline springs (Wadi 2.9 to 3.2 Ca-chloride type with low Na/Cl and 27 el Maliach) SO4/Cl ratios
Southern Section
Zarqa saline springs emerging 4.2 to 16.0 Mg-chloride with high Na/Cl and SO4/Cl 37; 40; 41 from the Jurassic and Lower ratios Cretaceous rocks Shallow springs and 2.5 to 15.5 Mg-chloride enriched in sulfate with high 39; 43; 45; groundwater emerging from the Na/Cl and SO4/Cl ratios, high nitrates 48; 51; 52 Pleistocene sediments
Hypersaline brines 60.0 to 86.6 Ca-chloride with low Na/Cl and SO4/Cl 42; 46 (53) (2.2 to 2.4) ratios
19 Table 3. Calculations of the mixing proportions between saline diverted water (“saline carrier”) and sewage effluents (“Bitaniya”) that compose the initial base flow of the lower Jordan River at Alumot Bridge. Calculations were made for different major elements.
ID name Date Ca (mM) f (%) Mg (mM) f (%) Na (mM) f (%) Cl (mM) f (%) SO4 (mM) f (%) JR-119 Saline carrier 12-2000 12.34 78 5.19 77 51.55 79 78.27 76 1.92 78 JR-118 Bitaniya 2.52 22 2.22 23 11.79 21 12.13 24 1.03 22 JR-117 Alumot Bridge 10.22 100 4.50 100 43.13 100 62.56 100 1.72 100 JR-149 Saline carrier 02-2001 12.74 60 5.23 61 51.11 64 77.99 61 1.88 64 JR-148 Bitaniya 2.55 40 2.18 39 11.4 36 12.47 39 1.00 36 JR-147 Alumot Bridge 8.67 100 4.03 100 36.97 100 52.46 100 1.56 100 JR-179 Saline carrier 03-2001 9.64 90 4.28 86 40.89 87 62.34 86 1.72 78 JR-180 Bitaniya 2.62 10 2.22 14 11.48 13 12.47 14 0.99 22 JR-178 Alumot Bridge 8.97 100 3.99 100 37.19 100 55.57 100 1.56 100 JR-224 Saline carrier 04-2001 10.84 85 4.69 61 46.11 83 67.55 83 1.80 85 JR-225 Bitaniya 1.44 15 3.74 39 11.96 17 13.37 17 0.92 15 JR-223 Alumot Bridge 9.44 100 4.32 100 40.45 100 58.39 100 1.67 100
20 70 May 2000 A 48 B May 2000 B B 65 46 A 44 ) 60 42 ) D A mM 55 C D 40 mM C 50 38 Cl ( 36 ( Na 45 34 0 5 10 15 20 25 30 0 5 10 15 20 25 30 11 7.0 May 2000 C ) B 10 B 6.5 mM
9 ) A A C D 6.0 Mg ( 8 mM C D 5.5
7 Ca ( 6 5.0 May 2000 D 0 5 10 15 20 25 30 0 5 10 15 20 25 30 5.5 0.090 ) A D
5.0 0.085 ) mM 4.5 ( 0.080 mM 4 A 4.0 0.075 B ( 3.5 SO 0.070 B C 3.0 B C D 0.065 2.5 0.060 2.0 May 2000 E 0.055 May 2000 F 0 5 10 15 20 25 30 0 5 10 15 20 25 30 0.90 March 2000 0.14 March 2000 0.85 D 0.12
B C (M/M) (Molar) (Molar) 0.80 (M/M) A 0.10 May 2000 /Cl 0.75 0.08 4 A June 2001 Na/Cl Na/Cl
SO D 0.70 June 2001 0.06 C 0.65 0.04 B May 2000 G H 0.60 0.02 0 5 10 15 20 25 30 0 5 10 15 20 25 30 A -Yarmouk B - W. Arab Distance from Alumot Dam (km) C - Teibeh D - Harod
Fig. 4. Major ion, Na/Cl and SO4/Cl ratio transects along the northern lower Jordan 2+ 2- 3+ River, sampled in May 2000. Note the gradual variations of Mg , SO4 , B , Na/Cl, - + and SO4/Cl, and the sharp decrease in Cl and Na after the confluence with Wadi Arab. Arrows mark the other major tributaries.
21 12 8 ) ) 11 mM mM 7 10 Ca ( Mg ( Mg 9 6 8 7 5 B 6 4 5 A A B
35 40 45 50 55 60 65 70 75 35 40 45 50 55 60 65 70 75
1.6 50 ) 1.5 ) mM mM 1.4 45 K (
1.3 Na (
1.2 40 1.1
1.0 35 0.9 C D 35 40 45 50 55 60 65 70 75 35 40 45 50 55 60 65 70 75 6 ) ) 0.10 mM mM
5 ( 4 Sr (
4 SO 0.08
3 0.06
2 B 0.04 A E F 35 40 45 50 55 60 65 70 75 35 40 45 50 55 60 65 70 75 Chloride (mM)
Fig. 5. Major elements versus chloride content in the northern section of the lower Jordan River. Arrow represents the river flow direction. Line A-B (graphs B and E) represents a mixture between sewage effluents and saline diversion water, which make up the base flow of the lower Jordan River downstream of Alumot Dam.
22 25 40 Yarmouk 20 Western Inflows 35 Eastern 15 Inflows (‰) 10 30 Yarmouk B (‰)
5 11 δ δ δ δ
sulfate Eastern 25 S 0 Inflows
34 Drainages δ δ δ δ 20 -5 A B -10 15 0 10203040506070 0 10203040506070
C Eastern inflowsD Western inflows 15 Saline Yarmouk Drainages Yarmouk + Drainages River
10 (mM) 4 Eastern Inflows SO
Western inflows 5
0 0 10203040506070
0.7090 Eastern 6 E Inflows 4 0.7085
(‰) 2 Sr Western Inflows 86 0.7080 0 water water Sr/ Drainages O -2
87 Yarmouk
0.7075 18 δ δ δ δ -4 Yarmouk D Hamadia Well -6 0 10203040506070 0 10203040506070 Chloride (mM)
34 87 86 18 11 Fig. 6. δ Ssulfate, Sr/ Sr, δ Owater, δ B values and sulfate concentration versus chloride content in the northern lower Jordan River (open circles), eastern inflows, western inflows, saline Yarmouk River, and drainage water. Hamadia well collects 18 shallow groundwater underlying fishponds and represents drainage of δ Owater- enriched effluents of overlying fishponds. Arrow represents the river flow direction.
23 25
20
15
(‰) 10
sulfate 5 S 34 δ δ δ δ 0 Yarmouk
-5 Eastern Inflows -10 0 0.1 0.2 0.3 0.4 0.5 0.6 0.7 1/SO (1/mM) 4 34 Fig. 7. δ Ssulfate values versus reciprocal of sulfate of the northern lower Jordan River (open circles), saline Yarmouk, and eastern inflows.
Using mixing equations, the relative proportions of the groundwater component in the northern lower Jordan River were determined. The equations assume that the concentration C(x) of conservative species in the river is determined by mixing with the groundwater component as follows:
C(x)=CYf(x)+Ci(1−f(x)) (1)
where Ci is the initial river concentration (downstream of Alumot Dam), CY is the concentration in the saline Yarmouk River (which is considered to be a good proxy for the groundwater composition) and f is the groundwater component discharge divided by the total river discharge. f values for each of the sampling months were calculated. Correlating f with distance from the river source (Alumot) was obtained by applying equation 1 using chloride concentration. Computed concentrations of sodium, sulfate and other species were then calculated as a function of f. Theoretical curves of ion ratio versus chloride concentration were finally plotted and compared with measured values. Figure 8 illustrates an example for Na/Cl, SO4/Cl, and Mg/Cl variations in the lower Jordan River during December 2000. The variations in these ionic ratios determined for the lower Jordan River water along the upper 12 km follow the theoretical mixing line between the initial river water and the saline Yarmouk
24 River. The different ionic ratios were found to yield similar results and the overall contribution of the groundwater discharge varied between 20 and 50% of the total river flow (measured at ~12 km downstream of Alumot Dam). In a parallel study, Shavit et al. (2002) and Holtzman (2003) applied flow-rate measurements and detailed water mass-balance calculations along small segments of the river. The flow- rate values obtained in the northern part of the lower Jordan River varied from 600 to 900 L/s. Thus, the mixing calculations in this study of groundwater discharge of 20 to 50% of the river flow infer a contribution of 120 to 450 L/s to the river.
2.1.2.2. Chemical modification in the central section
In the central segment, 20 to 60 km aerial distance from Alumot Dam, the sampling points were limited for logistic and security reasons. In addition, the monitoring sites for surface-water inflows and groundwater on the two sides of the river were uneven, with a large number of inflows on the eastern side and only a few on the western side (Table 2 and Fig. 1). In contrast to the northern and southern sections, only minor salt- content variations were observed in the lower Jordan River water here, despite a 87 86 significant downstream increase of the Sr/ Sr and SO4/Cl ratios (Fig. 3). The major western inflow in this area is Wadi el Maliach, with chloride concentrations of 36 to 87 86 42 mM, Sr/ Sr of 0.70776, and SO4/Cl of 0.08 to 0.1. In contrast, the eastern inflows and groundwater have a chloride range of 2.8 to 48 mM, 87Sr/86Sr of 0.7080 to 87 86 0.7087, and SO4/Cl ratios of 0.01 to 0.8 (Table 2). The increase in the Sr/ Sr and
SO4/Cl ratios observed in the river indicates that the eastern inflows have major control over the chemical and isotopic compositions of the river water while the 87 86 western inflow, with lower Sr/ Sr and SO4/Cl ratios, is negligible. Predominance of agricultural activity and relative richness in water resources along the eastern side result in surface-water flow and modification of the lower Jordan River along this segment.
25 Table 4. A summary of the major geochemical features (isotopic composition and ionic ratios) characterizing the major water sources in the northern section of the Jordan valley. The different geochemical parameters are compared with the postulated “end member” that directly controls the Jordan River water.
Calculated End Member Saline Yarmouk Eastern Inflows W, Teibeh Fish Ponds Western Inflows Cl (mM) < 34 23-45 < 20 15-21 45-71 28-71
SO4 (mM) > 5.5 5.5-11 0.5-5.5 14-17 2.5--6.5 2-13 Na (mM) < 30 22-37 1-11 17-18 30-49 28-49 Mg (mM) > 6 6-12.5 1-4.5 9-12.5 6.5-10 5-12 Ca (mM) < 5 3.5-5 1.5-4 6-8.5 3.5-8.5 5-8.5 Na/Cl > 0.8 0.85-0.95 1 0.8-1.2 0.62-0.77 0.68-0.75
SO4/Cl > 0.12 0.23-0.26 0.2-0.3 1 0.05-0.11 0.05-0.07 87Sr/86Sr < 0.7075 0.7072 0.7076-0.7087 0.7079 0.70762 0.70741-0.70791 δ11B 28-36 ‰ 36 ‰ 28 ‰ 21 ‰ 31.5 ‰ 22-43 ‰ δ34S < 5 ‰ (-2) ‰ (-4)-(-5) ‰ (-5.4) ‰ No Data No Data Legend: White boxes---possible agreement with changes observed along the northern section of the lower Jordan River. Gray boxes---inconsistent data with changes observed along the northern section of the lower Jordan River.
26 Yarmouk Fraction (%) 100 60 40 20 0 0.30 Yarmouk A December 2000
0.25 Measured Values Calculated Values 0.20
0.15
Mg/Cl (M/M) Initial River 0.10 Chloride (mg/L) 0.05 1000 2000 Yarmouk Fraction (%) 100 60 40 20 0 0.95 Yarmouk B 0.90
0.85
0.80 Initial
Na/Cl (M/M) 0.75 River
0.70 Chloride (mg/L) 0.65 1000 2000 Yarmouk Fraction (%) 100 60 40 20 0 0.25 Yarmouk C
0.20
0.15 /Cl (M/M) 4 0.10 Initial SO River 0.05 Chloride (mg/L) 0 1000 2000
Fig. 8. Mg/Cl , Na/Cl and SO4/Cl ratios versus chloride concentrations in the upper 12 km of the lower Jordan River sampled during December 2001. The measured data (black triangles) are compared to a theoretical mixing line between the initial river at Alumot Dam and the saline Yarmouk River as sampled in that month. Note the increasing fraction of the groundwater component, represented by the composition of the saline Yarmouk, along the flow of the lower Jordan River.
27 2.1.2.3. Chemical modification in the southern section
The southern section of the Jordan River (60 to 100 km from Alumot Dam) is characterized by a downstream increase in salt contents (Fig. 9). Overall, the contents of all of the dissolved solutes increase linearly with chloride (Fig. 10). Seasonal variations were observed in the intensity and locations of chemical modifications accompanying this salt increase. During fall and winter, the salt content in the lower Jordan River rises gradually downstream, but its magnitude is small (a chloride increase of only 9 mM between Adam and Abdalla bridges; Fig. 1). During the spring months, the lower Jordan River has a saline peak (TDS up to 6000 mg/L) at a distance of 70 to 80 km downstream of Alumot Dam. During the summer months, the salt content increases continuously with distance (TDS of 11090 mg/L in August 2001) before the river enter the Dead Sea (Fig. 9A). The changes in the dissolved-salt patterns are also associated with changes in chemical compositions. The Jordan River water at a distance of 60 to 90 km downstream of Alumot Dam is characterized by
Na/Cl > 0.75 and SO4/Cl > 0.145. Further south, at a flow distance of >90 km, the rise in salt content is associated with Na/Cl < 0.75 and SO4/Cl < 0.145 (Fig. 11). In contrast to the large variations in the total dissolved salts, the isotopic values of 87 86 34 18 15 Sr/ Sr, δ Ssulfate, δ Owater (Fig. 3) and δ Nnitrate (Table 1) vary only marginally in the lower part of the Jordan River, except for a slight increase in the 87Sr/86Sr ratio at a flow distance of 66 to 75 km (i.e., Adam Bridge, 87Sr/86Sr = 0.70803-0.70815). A detailed survey of all eastern and western wadis flowing into the lower Jordan River and groundwater near the southern Jordan Valley (Table 1) reveals that the inflows in the southern section include brackish water from the Zarqa River and two types of groundwater: one is a brine represented by Wadi Ah’mar (on the west) and Aqraa (on the east), having the typical Ca-chloride composition of the Dead Sea Rift valley (Starinsky, 1974; Stein et al., 1997), and the other is a sulfate-rich saline spring (e.g., Mallaha and Bassat El Faras on the eastern side) that represents groundwater (Table 2). The brackish water of the Zarqa River is derived from natural saline springs that emerge within the Jurassic and Lower Cretaceous rocks and is characterized by 87 86 11 Na/Cl ~ 0.9, SO4/Cl ~ 0.25, high Sr/ Sr (~0.7087), and relatively low δ B (~25‰;
Fig. 12). The brines have low Na/Cl (0.55-0.69) and SO4/Cl (0.02-0.04), high Br/Cl (5-9×10-3), and δ11B > 40‰ (Table 2) values. In contrast, the sulfate-rich groundwater -3 11 has high Na/Cl (0.8-1.0), SO4/Cl (0.25-0.5), low Br/Cl (1-4×10 ), and δ B ~ 30‰ values. This type of saline groundwater has been identified in the Jericho area near the
28 southern end of the river (Marie and Vengosh, 2001). Both groundwater and brines 87 86 34 have Sr/ Sr ratios of ~ 0.7081 and δ Ssulfate values of 4‰ to 10‰ (Table 1 and Fig. 12). The variations in dissolved-salt content, the chemical modifications along the river, and specific chemical and Sr isotopic mass-balance calculations using water before and after the confluence of the Zarqa River with the lower Jordan River clearly indicate that the source of the salts in the southern section of the river cannot be explained by a single surface inflow, or by net evaporation of the river along its flow. The latter is evidenced by the changes in the ionic ratios along the flow (Fig. 11) and 18 the lack of a significant increase in δ Owater values that would accompany a rise in salt content due to evaporation (Fig. 3). Figure 13 illustrates a linear correlation (R2 = - 2- 0.912) between Cl and SO4 , indicating a single source for the dissolved salts. The composition of this source appears to be different, however, from those of the brines or sulfate-rich groundwater. Hence, none of the three water inflows can be the sole source affecting the river's water quality. 34 The δ Ssulfate values in the river (5-7‰) are similar to those of the three major water sources, the Zarqa River (9‰), the brines, and sulfate-rich groundwater (4-10‰; Table 2 and Fig. 3), and hence cannot be used to detect the relative contributions of these sources. The 87Sr/86Sr and δ11B variations (Fig. 12) show that the brines and sulfate-rich groundwater have similar 87Sr/86Sr ratios (0.7081) but differ in their δ11B values as the brines are characterized by δ11B > 40‰. In contrast, the Zarqa River has high 87Sr/86Sr (0.7087) and low δ11B (~25‰) values. 18 The constant downstream δ Owater values of the southern Jordan River (Fig. 3D) confirm that the rise in salt content is not derived only from evaporation processes, 18 which would result in an increase of the δ Owater. In contrast, all of the groundwater 18 analyzed yielded low δ Owater values (<-4‰; Table 2). Hence, it seems that the 18 δ Owater values recorded in the river reflect a balance between groundwater discharge 18 18 (low δ Owater) and residual evaporation (high δ Owater).
29 6000 A
5000 Summer- August 2001 4000
August 2000 3000 Spring Cl (mg/L) Cl
2000 Winter
1000 60 65 70 75 80 85 90 95 100
50 B March 2000 40
30 March 2001 (mg/L)
3 May 2000
NO 20
June 2001 10
60 65 70 75 80 85 90 95 100 Distance from Alumot Dam (km)
Fig. 9. The variation of chloride (A) and nitrate (B) contents with flow distance along the southern lower Jordan River as recorded during winter, spring, and summer (sampled on 4 of 14 field trips).
30 120 20
100
15 (mM) 80 4 Na (mM) SO 60 10
40 Cl (mM) 5 Cl (mM)
40 60 80 100 120 140 40 60 80 100 120 140 15 0.25
0.20
10 B (mM) Ca (mM) 0.15
0.10 5 Cl (mM) Cl (mM)
40 60 80 100 120 140 40 50 60 70 80 90
0.16 1.2 0.14 1.0 0.12 0.8 Sr (mM) 0.10 Br (mM) 0.6 0.08 0.4 0.06 0.04 Cl (mM) 0.2 Cl (mM) 40 60 80 100 120 140 40 60 80 100 120 140 30
25
20 Mg (mM) Mg 15
10 Cl (mM)
40 60 80 100 120 140 Fig. 10. Major elements versus chloride content in the southern lower Jordan River. The arrow represents the flow direction of the river. Note the linear relationships between most of the dissolved salts and chloride, indicating that a mixing process controls the water salinity of the Jordan River.
31 June 2001 June 2001 100 0.84 100 0.160 0.155 90 0.82 90 SO4/Cl Na/Cl Cl (mM) 0.150 80 0.80 80 (mM) Cl 0.145 70 70 0.140 0.78 /Cl (M/M) 60 60 4 0.135 0.76 50 Na/Cl (M/M) 50 SO 0.130 0.74 0.125 A 40 B 40 0.120 0.72 60 65 70 75 80 85 90 95 100 60 65 70 75 80 85 90 95 100 August 2001 August 2001 0.16 160 0.80 160 Na/Cl 140 140 0.15 SO4/Cl Cl (mM) Cl (mM) Cl 120 0.75 120 0.14 100 100 /Cl (M/M) 4 80 0.13 80 0.70 Na/Cl (M/M) SO 60 0.12 60 C 40 D 40 0.11 0.65 60 65 70 75 80 85 90 95 100 60 65 70 75 80 85 90 95 100
Distance from Alumot Dam (km)
Fig. 11. Chloride concentration, SO4/Cl, and Na/Cl ratio transects along the southern lower Jordan River sampled in June and August 2001. Note the different chemical compositions of the river before and after a distance of ~90 km from Alumot Dam.
32 0.7088 River Zarqa Eastern inflows Western inflows 0.7086
0.7084 Sr 86
Sr/ 0.7082
87 Pleistocene sediments
0.7080 Brines + Western inflows 0.7078 20 25 30 35 40 45 50 δ11 B (‰) Fig. 12. 87Sr/86Sr versus δ11B ratios of the southern lower Jordan River and the three major sources in the southern Jordan Valley. Note the relatively high 87Sr/86Sr ratios and low δ11B in the Zarqa River, which has only a minor impact on the composition of the Jordan River. The isotopic composition of the Pleistocene (Lisan) sediments (data from Stein et al., 1997) controls the composition of both the sulfate-rich groundwater and the lower Jordan River.
Fig. 13 illustrates that the salt content of the lower Jordan River is not derived from the individual saline inflows (i.e., brines or sulfate-rich groundwater) but rather from a saline groundwater that itself is a mixture of the sulfate-rich groundwater and brines. The strontium (87Sr/86Sr ~ 0.7081) and boron (δ11B ~ 30‰) isotopic compositions of the lower Jordan River are also consistent with this interpretation. Given that the absolute salt concentration and chemical composition of this groundwater source is unknown, the ionic ratios measured for the Jordan River water were used to estimate the chemical composition of this end member. It was hypothesized that the chemical composition of the groundwater that is discharged directly into the lower Jordan River lies along a mixing line between the brines and the sulfate-rich groundwater. Hence, the possible mixing line (Line 3 in Fig. 14) was initially calculated between these two sources. The highest chloride values and average ionic ratios measured were used for the sulfate-rich groundwater and brines as proxies for these two water sources. Subsequently, possible mixing scenarios were calculated between the postulated groundwater source and the Jordan River water for the specific salinization events in the spring (Line 1 in Fig. 14) and summer (Line 2 in Fig. 14). Calculations were
33 performed separately for two areas: Zarzir-Tovlan sites in the north (60-72 km downstream from Alumot Dam) and Allenby Bridge-Abdalla Bridge sites in the south (91-100 km; Fig. 1). In each area, the northern site (Zarzir or Allenby Bridge) was considered the "upstream river" and the southern (and saline) sites (Tovlan or Abdalla Bridge) as the "downstream river." Mixing equations were employed for different - + 2- - dissolved constituents (e.g., Cl , Na , SO4 , Br ), using the solute contents measured in the "downstream river" as the mixing products between the "upstream river" and an unknown saline "end member". The calculations point to a single solution for the mixing equations (M1 and M2 in Fig. 14), indicating a groundwater source with chloride of ~282 mM at the Tovlan site (72 km) and ~564 mM at the Abdalla site (100 km). Consequently, the estimated groundwater contribution to the lower Jordan River based on the solute mass balance at both sites is ~10%. It should be noted that these calculations show that the chemical composition of the groundwater inflows are different at the two sites. At the northern site, the mixed end member (Cl- ~ 282 mM;
M1 in Fig. 14) is characterized by higher Na/Cl and SO4/Cl ratios and reflects a mixture of 88% of saline groundwater with 12% brine. At the southern site, the higher salt content of the postulated mixing end member (Cl- ~ 564 mM; M2 in Fig. 14) reflects a larger fraction of brine, e.g., 60% groundwater and 40% brine. Since the groundwater and brine differ in their δ11B values (~30‰ and >39‰, respectively), the mixing calculations were tested using boron isotopic values. The available δ11B values determined for the Tovlan site (30-32‰) are consistent with the expected δ11B range upon mixing calculations made for the major dissolved solutes. It can be concluded that the volumetric contribution of the groundwater discharge to the lower Jordan River is low (10%), but due to the high salt content of this source, its impact on the water quality of the lower Jordan River is significant. Consequently, the dissolved salts at the southern end of the Jordan River are controlled by the relationship between the seasonally variable surface discharge and the relatively constant groundwater inflow. In the winter, a surface discharge of ~1660 L/s corresponds to a chloride content of ~56 mM, whereas in the summer a significant drop in the river discharge (370 L/s; Holtzman, 2003) results in increasing chloride content, up to 152 mM (Tovlan site).
34 50
Saline Hypersaline 30 Groundwater Brines (mM) 4 SO 10 R2 = 0.9120 8 River
6 Eastern inflows Western inflows
10 100 1000 Cl (mM)
Fig. 13. Log sulfate versus log chloride contents of the Jordan River as compared to the sulfate-rich groundwater and brines. Arrow represents the river flow direction. - 2- Note that the linear relationship between Cl and SO4 contents in the lower Jordan River was obtained on a linear scale. The log-log presentation only illustrates that the saline source that controls the river salinity is, itself, a mixing product between the brines and the sulfate-rich groundwater.
35 0.25 End - member
0.20
3
e Allenby 1 Zarzir in Line 0.15 L Tovlan April 2001 M1 Abdalla 2 /Cl (Molar) 0.10 e 4 in L August 2001 SO
0.05 Measured Values- April 2001 M2 Measured Values- August 2001 Brine Calculated Values 0 0 0.005 0.010 0.015 0.020 0.025 1/Cl (1/mM)
Fig. 14. SO4/Cl ratios versus the reciprocal of chloride in two salinization events in spring (Line 1) and summer (Line 2) along two segments of the southern Jordan River (see locations in Fig. 2). Line 3 represents the mixing relationships between the hypersaline brines (Cl- = 40,000 mg/L) and sulfate-rich groundwater (Cl- = 6,000 mg/L). Note that the chemical data measured in the river is used to constrain possible saline groundwater end members, M1 in spring and M2 in summer, which are discharged and affect the salinity of the river.
2.1.3. Conclusions The results revealed three distinct zones of salt-content changes along the lower Jordan River. Integration of hydrological, chemical, and isotopic (strontium, boron, sulfur, nitrogen, oxygen) data from the lower Jordan River and its tributaries enabled us to elucidate the different sources controlling the water quality of this part of the river. Using solute mass balances, we show that none of the identified tributary inflows can be a sole source for the high dissolved salt contents of the lower Jordan River. Instead, its water quality is controlled to a large degree by groundwater discharge. In the northern section, the groundwater contribution was estimated to vary between 20 and 50%. The discharge of the shallow sulfate-rich groundwater affects the water quantity and quality of both the Yarmouk (downstream from Adassiya Dam) and lower Jordan rivers. Chemical and isotopic data suggest that the shallow groundwater
36 is derived from a blend of agricultural drainage water, groundwater flow from the 34 eastern tributaries (with low δ Ssulfate < 0‰), and an unknown saline source with a low 87Sr/86Sr ratio (<0.7072). In the southern section of the lower Jordan River, seasonal salinization events were observed in the spring (TDS up to 6 g/L at a flow distance of 70-80 km) and summer (up to 11 g/L at the southern end of the river). The chemical and isotopic compositions of three major sources were characterized: (1) the Zarqa River; (2) sulfate-rich saline groundwater, and (3) subsurface brines. It was shown that none of these sources alone can explain the salinization trend in the lower Jordan River, but that variable mixtures of the two latter sources could explain the observed chemical variations. The chemical variations in the river were used to constrain the mixing proportions of these two sources and consequently derive possible mixing relationships between the discharged groundwater and the river. The mixing simulations show that the groundwater that flows into the southern lower Jordan River is saline (chloride between 282 and 564 mM). Although the contribution of the groundwater to this part of the river is estimated at only ~10%, its impact on salt content is significant. These data show that the water quality of the lower Jordan River has deteriorated due to a combination of a significant reduction in annual flow (from ~1300 MCM to 30– 200 MCM), the dumping of diverted saline springs and wastewater, and discharge of shallow saline groundwater. Mass-balance calculations show that in the northern section, the groundwater component is high (20 to 50% of the river flow), whereas in the southern section it is relatively low (~10%). Nevertheless, the latter section the Jordan River is much more saline, due to an increased component of brine. Shallow groundwater and deep Ca-chloride brines are shown to be the two dominant factors controlling the chemical and isotopic compositions of the lower Jordan River. In light of this finding, the next chapter discusses the geochemistry of shallow groundwater in the research area and its relationship with deep Ca-chloride brines.
37 2.2. The geochemistry of groundwater resources in the Jordan Valley: the impact of the Rift Valley brines
2.2.1. Introduction Water resources in the Jordan Rift Valley are influenced by mixing with deep brines that have a typically Ca-chloride composition (Starinsky, 1974). For example, the salt budget, and hence the chemical composition of the Sea of Galilee (Simon and Mero, 1992; Kolodny et al., 1999; Nishri et al., 1999) and the Dead Sea (Starinsky, 1974; Stein et al., 1997; Gavrieli et al., 2001) are largely controlled by mixing with these deep brines. Although these brines likely influence the salinity and chemical composition of groundwater between the Sea of Galilee and the Dead Sea, their role in this area has not been fully investigated. Here, the chemical and isotopic compositions of shallow groundwater in the lower Jordan Valley, between the Sea of Galilee to the north and the Dead Sea to the south, were investigated (Fig. 15). The objectives of this chapter are to characterize the chemical composition of shallow groundwater as well as to evaluate the impact of deep saline brines on the geochemistry of shallow groundwater in the Jordan Valley. To achieve these goals, large geochemical and isotopic databases were used, that is composed of major and minor ions distributions, strontium (87Sr/86Sr), boron (δ11B), sulfur (δ34S), and nitrogen (δ15N) isotopes. The variations of strontium isotopic ratios in groundwater provide useful information on the aquifer rocks in which the groundwater has been interacted. Given the lack of isotopic fractionation during water-rock interactions it is possible to trace and reconstruct the groundwater flow paths in different geological terrains (e.g., Bullen et al., 1996). In the Jordan Valley, three types of distinctive lithological aquifers are expect to trace: (1) basaltic aquifers in the northern area with a low 87Sr/86Sr signal (0.704; Stein et al., 1993); (2) sandstone aquifers with a potentially high 87Sr/86Sr ratio in the eastern part of the central Jordan Valley, associated with the exposure of the Triassic and Lower Cretaceous sandstone formations (Salameh, 2002); and (3) sediments of the Lisan and Samra formations within the central and southern Jordan Valley with a 87Sr/86Sr narrow range of 0.7078-0.7080 (Stein et al., 1997). The second sets of geochemical tools that are used here provide information on the origin of the dissolved salts in the investigated groundwater; in particular the distinction between mixing with the Rift
38 Valley brines (Starinsky, 1974) and dissolution of salts in the host sediments of the Jordan Valley (Katz and Kolodny, 1989).
Alumot N Deganiya Dam Syria Saline Sea of Dam Sea of A Galilee Galilee Carrier Israel Jordan Waste Yarmouk A Water River 0 Addasiya River
Dam Lower Jordan Dead 10 Sea Distance from the Sea the Sea of Galilee (km) from Distance Northern Boreholes Wadi Arab 03 40 30 20 Wadi Teibeh B1
25 km Jordan Valley boundary 50
Zarqa River 60 C B2 Legend
08 90 80 70 Dam Water group Southern Borehole area Boreholes Central Brine B3 B3 Valley boundary B A’ A 100 Jordan Valley A’ Dead A Jordan River
Sea Cr Fill J R Pe
Fig. 15. (A) Schematic map of the research area with the geographic location of brine samples, shallow boreholes and the different water groups in the Jordan Valley; (B) schematic geological cross section of normal faults existing both in the valley’s margins and the valley itself, adjacent to the river (after Garfunkel and Ben-Avraham, 1996); and (C) location map of the Jordan Valley.
39 The Rift Valley brines are characterized by low Na/Cl and SO4/Cl ratios and high Br/Cl, δ11B, and δ34S values (Starinsky, 1974; Vengosh et al., 1991b; Gavrieli et al., 2001). In contrast, halite and gypsum dissolution produce saline water with high
Na/Cl (~1), and SO4/Cl and low Br/Cl ratios. The fractionation of boron isotopes during salt precipitation (Vengosh et al., 1992) enables a distinction between residual brine (e.g., the Dead Sea brine with δ11B=57‰) and salt dissolution (δ11B<30‰). In contrast to the high δ34S values (>20‰; Gavrieli et al., 2001) measured in the Rift Valley brines, disseminated (secondary) gypsum within the aragonites of the Lisan or Samra formations is characterized by low δ34S values (as low as -26‰; Gavrieli et al., 1998; Torfstein et al., 2005). Thus the sulfur isotopic data may also provide important information on the mechanism of salt accumulation in the investigated groundwater. The third set of isotopes is related to anthropogenic influence, in particular contribution of sewage effluents and agricultural return flows that are characterized by distinctive nitrogen isotopic ratios (δ15N). Segal-Rozenhaimer et al. (2004) showed that shallow groundwater in the northern Jordan Valley has high δ15N values (~15‰) that can be derived from sewage effluents and/or animal waste. Nitrogen fertilizers have typically a lower δ15N signature. Likewise, the boron isotopic composition of sewage effluents is typically low (δ11B range of 0 to 10‰) and thus a useful tracer for delineating groundwater contamination by anthropogenic sources (Vengosh, 2003). Two data sets were use in this chapter. The first comprises the chemical composition of shallow groundwater derived from boreholes drilled in the northern and southern parts of the Jordan Valley, collected during the years 2003 to 2005. The second data source includes the chemical and isotopic compositions of groundwater sampled in springs and streams in the Jordan Valley, collected from 2000 to 2004. Through an evaluation of these data sets it was shown that deep brines influence the quality and chemical composition of shallow groundwater in the Jordan Valley. Saline brines have been recognized along the Jordan Valley in previous studies (Bentor, 1961; Goldschmidt et al., 1967; Neev and Emery, 1967; Zak, 1967, 1997; Freund et al., 1970; Begin et al., 1974; Starinsky, 1974; Katz et al., 1977; Garfunkel, 1981; Stein et al., 1997; Stanislavsky and Gvirtzman, 1999; Krumgalz et al., 2000; Moise et al., 2000; Stein et al., 2000; Klein-Ben David et al., 2004). These studies focused mainly on saline brines located around the Sea of Galilee (“the northern brines”) and the Dead Sea (“the southern brines”). However, limited data has been reported for the central section of the Jordan Valley ("the central brines").
40 Starinsky (1974) characterized the saline brines in the Jordan Valley as Ca-chloride
[Ca>(SO4 + HCO3)] type. Ca-chloride brines typically have low Na/Cl and high Br/Cl ratios, and are relatively depleted in sulfate and carbonate ions. The mechanism of formation of the deep saline brines has been evaluated in several studies (Neev and Emery, 1967; Zak, 1967; Starinsky, 1974; Stein et al., 1997, 2000; Gavrieli and Stein, in prep.). It has been proposed that during the Neogene, seawater penetrated into the Jordan Valley and formed several isolated water bodies. Since the Neogene, these water bodies have been captured in different areas along the tectonic depression of the Jordan Valley: the marine Sedom lagoon (late Pliocene to early Pleistocene), the continental lakes Amora and Lisan (Pleistocene), and the modern Dead Sea. Starinsky (1974) explained the origins of the chemical composition of the brine as the consequence of two major processes: (1) seawater evaporation beyond the halite- saturation stage and halite precipitation, which produced a decreased Na/Cl ratio increased Br/Cl ratio in the residual brines; and (2) dolomitization reactions of the Mg-rich brines with carbonate rocks and Ca-Mg exchange, leading to gypsum precipitation producing the Ca-rich brines. The residual brines infiltrated into the sediments of the Jordan Valley and the surrounding country rock, where dolomitization continued and mixing with meteoric water took place. The brines along the Jordan Valley were found to be the dominant factor controlling the water composition of the Sea of Galilee and Dead Sea. In the Sea of Galilee, 90% of the dissolved salts are derived from saline springs which supply less than 10% of the lake water (Simon and Mero, 1992; Kolodny et al., 1999). Likewise, the salinity and chemical composition of the Dead Sea (~219 g Cl/L; Gavrieli et al., 2001) and its precursor, Lake Lisan (100-300 g Cl/L; Stein et al., 1997) is derived from the discharge of the Ca-chloride brines to the surface of the rift valley (Starinsky, 1974; Stein et al, 2000; Gavrieli and Stein, in prep.). In the previous section it was established that subsurface contributions could explain the large variations in the salinity of the lower Jordan River, showing that groundwater plays a key role in affecting the water quality along different river sections (chapter 2.1). However, the characteristics and origin of the subsurface groundwater were not determined directly. The northern (up to 20 km downstream of Alumot Dam) and southern (60 to 100 km downstream of Alumot Dam) sections of the lower Jordan River are the area most affected by groundwater influx (Farber et al., 2004). In light of these findings, piezometers were installed in these areas to sample
41 the shallow groundwater and to determine its chemical and isotopic compositions. Shallow boreholes (with a depth of up to 20 m) were drilled in cultivated fields on the west bank of the lower Jordan River. The boreholes were drilled in two groups: one, composed of seven boreholes, is located in the northern part of the valley (10-20 km south of the Sea of Galilee and up to 1000 m west of the river; Fig. 15). The second, comprised of eight boreholes, is located in the southern part of the valley (72-77 km south of the Sea of Galilee and up to 450 m west of the river; Fig. 15). These boreholes penetrate different Quaternary sedimentary layers. In the northern boreholes, the lithology of the drilled material is divided into four major layers: red loam at the top followed by clay, sand, and basalt mixed with carbonate conglomerate of different thicknesses. The piezometers were perforated (4-10 m long of screen) in the permeable units (i.e., sand and gravel). In six of the seven boreholes in this area, the water table was 2 to 6 m below ground surface. The southern boreholes were drilled within the Quaternary sediments of the Samra Formation, part of the Dead Sea Group (Fig. 16), which includes clay, sand and conglomerate units. The permeable units (i.e., sand and conglomerate) lie between low-permeablity layers of clay (Fig. 16). In the southern group of boreholes, the water table was detected ~4 m below ground surface.
42 N Syria Upper Sea of
Jordan River Y ar Galilee mo uk Israel
Tovlan- cross section Palestinian Authority Jordan
West East JordanLower River
Dead Sea
Lisan Lisan The three 25 km Formation gypsums .
Jordan River Samara Samara Dead Sea Group Formation Borehole Borehole T-2 T-4 Clay Soil Water level Sand
Conglomerate 20 m 20
Clay
Fig. 16. Schematic hydrogeological cross section based on the southern boreholes in Tovlan, 72 km downstream of Alumot Dam.
43 2.2.2. Results Groundwater data in this paper are reported from two sources: (1) new shallow boreholes and (2) springs and streams.
2.2.2.1. The chemical composition of shallow boreholes in the northern section
The chemical composition of water sampled from the shallow boreholes during the years 2003 to 2005 is presented in Table 5. Based on this data, three different water types were identified: (1) Ca-chloride ((Ca/[SO4 + HCO3]) >1); (2) Na-chloride (Na/Cl > 1); and (3) Mg-chloride (Na/Cl < 1 and (Cl-Na)/Mg < 1). All groundwater samples from the northern boreholes are characterized by a Ca/Mg ratio lower than 1. The Ca-chloride-type water is characterized by chloride concentrations of ~6000 mg/L, low Na/Cl and SO4/Cl ratios (0.6-0.7 and ~0.02, -3 respectively), high (5 x 10 ) Br/Cl and high (>1) Q (i.e., Ca/[SO4 + HCO3]) ratios. The Na-chloride-type water is characterized by low salinity (~850 mg Cl/L), high -3 Na/Cl and SO4/Cl ratios (>1 and ~0.3, respectively), low (2.5 x 10 ) Br/Cl and low (<1) Q ratios. The Mg-chloride-type water is characterized by intermediate values relative to the two other water types, with chloride concentrations of ~4000 mg/L, a -3 Na/Cl ratio of ~0.72, a SO4/Cl ratio of ~0.15, a Br/Cl ratio of ~3 x 10 and Q <1.
Overall the Na/Cl and SO4/Cl ratios decrease with the salinity of the groundwater.
44 Table 5. Chemical and isotopic compositions of representative samples from the Jordan Valley groundwater near the lower Jordan River, between the Sea of Galilee and the Dead Sea. - Br - 3 NO - 3 HCO 2- 4 SO - Cl + K + Na 2+ Mg 2+ Ca S 34 δ Sr 86 Sr/ 87 B 11 ‰ ‰ mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L δ (m) Well depth depth Well Alumot (km) Distance from name north Boreholes- Date Type Water Bor-1Bor-1Bor-1Bor-4Bor-4Bor-4Bor-4Bor-6Bor-6 10.0Bor-6 10.0Bor-6 10.0 south Boreholes- 13.6G-1 13.6G-1 9.0 13.6G-1 9.0 13.6G-2 9.0 18.6 15/10/2003G-2 5.9 Na-chloride 18.6 09/03/2004G-2 5.9 Na-chloride 18.6 22/02/2005G-3 5.9 Na-chloride 18.6 15/10/2003G-3 5.9 Ca-chloride 09/03/2004G-3 5.0 Ca-chloride 22/02/2005G-4 76.6 5.0 Ca-chloride 25/10/2004G-4 5.0 76.6 Ca-chloride 15/10/2003T-1 5.0 76.6 Mg-chloride 09/03/2004T-1 76.6 Mg-chloride 22/02/2005T-2 76.6 Mg-chloride 15.5 25/10/2004T-2 76.6 Mg-chloride 15.5 134T-3 76.6 15.5 163 15/11/2004 154T-3 76.6 Ca-chloride 14.0 117 03/01/2005 142T-4 76.6 620 Ca-chloride 14.0 345 26/04/2005 121T-4 76.6 660 Ca-chloride 14.0 347 11 15/11/2004 595 76.6 585 Ca-chloride 10.0 281 03/01/2005 630 8 2620 72.4 880 Ca-chloride 10.0 303 26/04/2005 527 7 2700 72.4 80 Ca-chloride 608 10.0 870 700 15/11/2004 557 2450 72.4 Ca-chloride 90 505 12.0 800 6132 595 03/01/2005 2700 780 72.4 Ca-chloride 90 327 375 12.0 6330 560 26/04/2005 1880 400 495 72.4 95 Ca-chloride 400 10.0 494 5622 26/01/2005 427 1810 400 30 72.4 31 Ca-chloride 10.0 298 6020 510 26/04/2005 440 1780 318 72.4 41 Ca-chloride 71 4286 288 1450 8.0 1850 09/11/2004 360 72.4 47 18 52 Ca-chloride 3980 6 1900 1650 293 1100 8.0 26/04/2005 50 Ca-chloride 3 3532 5500 1450 1600 300 1150 8.0 5 509 09/11/2004 3 3737 4200 1483 1300 72 150 3000 8.0 Ca-chloride 4 495 26/04/2005 10 4212 15260 11.5 3900 1500 100 21 3200 Ca-chloride 75 586 15/11/2004 11850 16.9 1700 11925 11.5 4550 100 3315 Ca-chloride 1 63 580 500 26/04/2005 14000 4200 1600 11404 4326 71 5000 15/11/2004 Ca-chloride 1 454 29 35000 5700 600 13770 1700 Ca-chloride 6300 26/04/2005 0 18500 359 1600 39718 555 19500 25 Ca-chloride 3980 920 561 1700 39335 900 21 166 5428 4850 5 53584 1900 56626 17340 28 339 10 7550 4750 2000 2000 835 20200 182 137 7673 2700 135 10 48546 159 945 21267 429 4400 120 2600 2100 20 61020 960 13700 4326 50 472 2500 62763 2850 568 600 13770 415 3750 2400 2570 37500 513 560 400 11250 758 4120 20 3150 4600 36391 166 420 11781 144 7000 708 2900 4260 325 31750 435 1850 15700 6746 20 592 3050 342 33400 2750 565 15300 777 860 3250 7660 52150 505 154 1195 20 830 2050 50047 180 3978 390 2000 22490 342 110 440 460 1800 20 439 10035 1400 359 387 20 418 461 702 660 10 269 116
45 Table 5 (Continued). 4 /Cl Br/Cl Sr/Ca Ca/SO 4 TDS Na/Cl Q Mg/Cl Ca/Mg SO 2+ Sr 3+ B mg/L mg/L mg/L mM mM mM mM mM mM mM mM (m) Well depth Alumot (km) Distance from from Distance Bor-1Bor-1Bor-1Bor-4Bor-4Bor-4Bor-4Bor-6 10.0Bor-6 10.0Bor-6 10.0Bor-6 13.6Boreholes- south 9.0 13.6G-1 9.0 13.6G-1 15/10/2003 9.0 13.6G-1 09/03/2004 Na-chloride 5.9 18.6G-2 22/02/2005 Na-chloride 5.9 18.6G-2 1.1 15/10/2003 Na-chloride 5.9 18.6G-2 09/03/2004 Ca-chloride 5.9 3.7 18.6G-3 22/02/2005 Ca-chloride 5.0G-3 2.0 25/10/2004 2861 Ca-chloride 5.0 4.8G-3 15/10/2003 76.6 Ca-chloride 5.0 4.0 1.09 9.1G-4 3126 09/03/2004 76.6 Mg-chloride 5.0G-4 10560 0.34 2621 22/02/2005 76.6 Mg-chloride 1.17 9.8 2.2T-1 25/10/2004 0.66 76.6 Mg-chloride 1.13 7.8 0.26T-1 15.5 10863 0.35 76.6 Mg-chloride 9.3 8.7 1.30T-2 15.5 0.33 9647 0.66 76.6 15/11/2004 0.53 0.24T-2 15.5 9609 10416 76.6 03/01/2005 0.14 9.5 Ca-chloride 0.67 0.22 1.33T-3 14.0 0.69 0.29 76.6 26/04/2005 7.5 0.68 0.70 Ca-chlorideT-3 14.0 9017 1.23 0.35 5.7 0.15 76.6 15/11/2004 7.8 0.59 2.8E-03 Ca-chloride 1.22T-4 14.0 0.71 8136 0.33 2.7 76.6 03/01/2005 0.70 0.013 Ca-chloride 31.0 0.14T-4 10.0 0.02 8655 0.33 0.23 3.0 76.6 26/04/2005 0.13 0.74 2.5E-03 0.20 Ca-chloride 27.0 0.46 26596 10.0 0.61 5.2E-03 7.0 15/11/2004 0.76 0.013 72.4 0.32 2.2E-03 Ca-chloride 25.0 20874 0.02 10.0 0.50 0.56 0.012 0.33 6.2 0.62 03/01/2005 0.016 72.4 0.21 Ca-chloride 75.0 0.50 20740 12.0 0.49 0.54 5.3E-03 7.0 0.02 26/04/2005 72.4 2.07 0.19 1.69 Ca-chloride 93.0 12.0 0.57 56488 0.02 13.5 0.013 0.14 0.57 0.55 26/01/2005 72.4 0.20 5.0E-03 1.40 Ca-chloride 87.0 64685 10.0 0.52 124.0 5.2E-03 0.18 26/04/2005 9.5 0.46 3.0E-03 0.013 2.08 72.4 1.29 Ca-chloride 63871 10.0 0.15 11.5 0.013 91463 0.54 0.18 0.007 0.48 Ca-chloride 72.4 09/11/2004 125.0 4.16 2.12 0.46 0.13 10.9 0.54 105.0 8.0 0.19 0.53 2.8E-03 72.4 26/04/2005 2.02 85871 3.90 0.88 11.0 Ca-chloride 0.46 0.15 79256 105.0 8.0 0.009 0.16 2.5E-03 72.4 3.96 Ca-chloride 105.0 0.53 0.04 5.13 09/11/2004 0.47 98386 10.0 8.0 0.009 0.17 0.55 3.3E-03 100829 0.76 0.05 26/04/2005 0.47 5.3E-03 Ca-chloride 8.0 4.74 0.009 0.16 0.51 9.5 0.52 62.0 0.16 0.69 0.06 3.93 15/11/2004 0.010 11.5 0.43 5.0E-03 Ca-chloride 11.0 62815 0.64 0.02 60.0 4.13 4.50 26/04/2005 0.16 0.011 11.5 0.47 4.7E-03 Ca-chloride 0.48 2.05 15/11/2004 0.16 7.5 0.02 55.0 0.56 0.010 61369 6.0E-03 Ca-chloride 1.65 0.18 0.18 26/04/2005 14.0 0.45 Ca-chloride 0.02 0.011 53611 0.01 6.3E-03 0.58 57.0 0.44 1.90 1.62 Ca-chloride 6.0 98.0 0.013 5.8E-03 0.38 0.55 0.39 5.5E-03 4.50 3.7 56384 0.01 1.97 0.012 0.17 83109 0.02 0.011 95.0 4.51 3.0 0.54 6.3E-03 2.16 52.0 0.01 0.02 0.46 5.4E-03 4.18 0.17 79977 6.00 0.014 0.37 24.0 37358 1.73 5.9E-03 0.012 5.7E-03 0.17 0.47 4.76 0.010 5.04 18165 0.36 0.010 0.53 0.03 4.55 0.18 4.36 0.46 0.61 4.75 0.20 4.65 2.13 5.2E-03 0.03 0.38 0.010 1.17 0.20 0.04 0.40 5.6E-03 0.18 0.011 2.06 5.4E-03 0.04 0.17 0.38 0.01 0.009 0.41 2.15 5.6E-03 0.44 6.0E-03 0.01 2.24 0.010 0.03 0.010 5.9E-03 1.90 0.05 5.3E-03 0.010 5.38 0.013 5.1E-03 5.11 0.013 2.47 1.47 Table 1 (Continued) nameBoreholes- north Date Water Type
46 Table 5 (Continued). - Br - 3 NO - 3 HCO 2- 4 SO - Cl + K + Na 2+ Mg 2+ Ca S 34 δ Sr 86 Sr/ 87 B 11 ‰ ‰ mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L δ Alumot (km) Alumot Distance from Distance from En HugaEn Spring Hasida Lower Spring Hasida GroundwaterTirtcha WellTirtcha Aqraa 20.9Aqraa 20.4 70.6Aqraa 20.35 KafrainHisban 24/05/2000 KafrainHisban Ca-chloride 98.8 24/05/2000Hisban 27/02/2001 70.6 24/05/2000 Ca-chloride Ca-chlorideAh'mar el Wadi Ca-chloride 41.21Ah'mar el Wadi 43.71Ah'mar el Wadi 01/12/2001 70.3 43.21 98.8 25/09/2000 0.70780Ah'mar el Wadi Ca-chloride Ca-chloride 70.3 98.8Ah'mar el Wadi 0.70783 70.3achmar el Wadi 75.0 27/02/2001 27/02/2001Group A 75.0 Ca-chloride Ca-chloride 09/04/2001 09/04/2001-Flood River Yarmouk 253 75.0 Ca-chloride Ca-chloride 01/12/2001Yarmouk River-Flood 167 75.0 Ca-chloride 246 29/03/2000 48.2 River Yarmouk Fresh 75.0 Ca-chloride 682 25/05/2000 151 48.6 River Yarmouk Fresh 6.3 75.0 Ca-chloride 27/02/2001 239 0.70802 River 25.6 Yarmouk Fresh 662 Ca-chloride 6.3 23/04/2001 158 0.70794 River Yarmouk Saline 1635 Ca-chloride 17.7 823 41.71 04/06/2001 2.6 River Yarmouk Saline 721 10.2 210 Ca-chloride 1560 2.6 27/04/2005 609 23/02/2003 B1 Subgroup 0.70796 Ca-chloride 23.9 Na-chloride 3.3 1970 342 1960 230 TeibehWadi 2370 03/02/2004 6.3 4500 1629 229 4590 Na-chloride TeibehWadi 4.3 214 660 12/04/2001 17000 344 6.3 16700 23 135 260 Na-chloride TeibehWadi 1150 1080 03/01/2002 5180 1055 3530 38230 Na-chloride 6100 03/01/2002 22 334 41500 1640 3976 344 11 4140 Na-chloride 01/09/1999 31.47 4190 13820 366 530 25.0 276 Mg-chloride 24/05/2000 1133 267 31.80 9 32 350 0.70693 14124 285 Mg-chloride 37900 0.70752 937 2020 32.80 16.5 645 283 36.20 3 500 1810 4160 755 0.70754 3650 10 16.5 285 15500 36.71 3885 725 322 0.70758 112 40.5 740 16.5 10.6 84 14050 0.70719 985 68 273 3580 57.0 2245 10.2 1010 0.70716 27/02/2001 38000 4060 40 37 3200 -2.1 0 545 76 37990 2005 Na-chloride 4100 82 14700 450 09/04/2001 3465 41 4870 1770 76 1110 Na-chloride 192 14 13100 494 01/12/2001 146 33 5250 293 630 3500 36 39630 Na-chloride 129 18800 980 34 8 3605 198 176 1730 36 1415 90 12954 36700 50 97 145 36 21 52896 630 25 122 1800 94 905 83 2550 69 206 7.0 5 470 30.6 7.1 15 36356 159 782 7.0 10 0.70790 702 1950 98 1041 122 19 20 145 50 40 20 135 117 -5.4 26.9 580 723 76 110 92 1130 40 575 4 80 451 306 20 660 322 710 307 242 144 298 468 16 52 432 10 423 12 244 9 40 9 56.0 10 1 220 1 553 151 271 1 10 0 412 1580 219 10 47.0 378 411 515 49.0 0 42 1330 520 3 1400 332 71 46 3 3 Table 1(Continued) Table nameCa-chloride Date Water Type
47 Table 5 (Continued). 4 /Cl Br/Cl Sr/Ca Ca/SO 4 TDS Na/Cl Q Mg/Cl Ca/Mg SO 2+ Sr 3+ B mg/L mg/L mg/L mM mM mM mM mM mM mM mM Alumot (km) Distance from from Distance En Huga Spring Hasida Spring LowerHasida GroundwaterTirtcha WellTirtcha Aqraa 20.9Aqraa 20.4 70.6 20.35Aqraa KafrainHisban 24/05/2000 Ca-chloride KafrainHisban 24/05/2000 27/02/2001 24/05/2000 70.6 Ca-chloride 98.8Hisban Ca-chloride Ca-chloride el Ah'marWadi 0.4 el Ah'marWadi 0.4 3.6 25/09/2000 01/12/2001 70.3 el Ah'marWadi 98.8 0.3 Ca-chloride Ca-chloride el Ah'mar 70.3Wadi 98.8 2.7 el Ah'mar 70.3Wadi 26.5 2.8 3349 2.8 27/02/2001 75.0 el achmarWadi 27/02/2001 10.0 10773 0.4 Ca-chloride Ca-chloride 3417 09/04/2001 75.0Group A 09/04/2001 3241 0.64 0.58 Ca-chloride Ca-chloride 01/12/2001 75.0 River -FloodYarmouk 0.68 13.0 Ca-chloride 0.65 1.27 29/03/2000 75.0 River -FloodYarmouk 3.0 1.06 20.6 23693 0.6 Ca-chloride 1.08 25/05/2000 75.0 River Yarmouk Fresh 20.7 0.15 1.18 2267 0.7 Ca-chloride 0.17 0.67 27/02/2001 River 6.3 75.0 Yarmouk Fresh 0.14 8.4 45.2 Ca-chloride 0.14 23/04/2001 0.92 River 6.3 Yarmouk Fresh 0.55 6.8 0.82 1.76 3.7 43.0 71034 Ca-chloride 04/06/2001 River 0.92 Yarmouk Saline 6.6 2.6 4.7 0.99 1.10 68497 Ca-chloride 4231 0.05 0.11 37.0 0.62 27/04/2005 River Yarmouk Saline 0.12 23/02/2003 12.6 2.6 Ca-chloride 4192 0.06 65.5 Na-chloride 0.69 65578Subgroup B1 0.21 3.0E-03 03/02/2004 0.52 0.05 3.3 1.36 5.8E-03 3.8 0.37 69.5 Na-chloride 63291 TeibehWadi 2.7E-03 6.3 0.56 0.63 0.005 1.09 12/04/2001 6.7 80.0 2.6E-03 0.015 1.03 1.95 0.16 62911 TeibehWadi 6.3 Na-chloride 0.02 12.0 0.57 0.005 03/01/2002 65522 0.1 1.33 2.89 0.005 1.12 61.0 0.17 TeibehWadi 1.20 0.19 Na-chloride 0.56 0.11 03/01/2002 0.31 6.0E-03 2.21 4.68 0.57 59999 0.21 2.56 Na-chloride 01/09/1999 0.16 66.0 0.27 3.8E-03 4.46 0.009 0.78 0.2 Mg-chloride 24/05/2000 0.3 0.55 0.04 0.15 4.70 59875 0.75 0.29 0.1 Mg-chloride 0.006 2.45 0.15 0.04 86649 0.07 5.8E-03 3.99 16.5 0.15 0.55 326 0.57 0.2 0.3 1.93 1.9 1.2 0.09 0.55 8.6E-03 0.04 0.009 16.5 4.0E-03 0.54 0.14 4.11 0.54 2.2 1.0 1.11 0.02 0.010 348 16.5 4.1E-03 5.5E-03 4.45 0.008 779 1.36 1.0 0.02 27/02/2001 0.14 0.56 9.1E-03 0.58 0.009 2.1 736 0.008 0.02 1.14 Na-chloride 1.19 1.95 0.14 09/04/2001 1.03 7.4E-03 2.1 0.008 733 0.59 Na-chloride 1.70 0.41 6.5E-03 3245 0.02 1.18 01/12/2001 1.14 0.54 0.009 0.56 0.59 Na-chloride 3371 4.95 0.010 1.07 7.0E-03 0.93 1.60 0.02 1.5 0.55 0.42 4.68 0.36 0.02 0.96 0.009 4.96 1.3 0.58 5.7E-03 0.32 0.39 0.30 1.46 1.5 5.5E-03 1.37 4.26 0.33 0.009 8.4 0.36 0.28 1.8E-03 1.41 9.3 0.28 0.27 4.30 0.23 2842 0.004 1.37 0.45 8.0 1.7E-03 0.23 3583 3.1E-03 0.43 1.23 2.22 0.22 3251 0.004 0.26 3.6E-03 4.58 1.18 0.007 0.36 0.23 3.3E-03 3.6E-03 1.22 0.006 2.16 2.12 0.39 3.9E-03 0.62 0.006 0.007 2.38 0.39 0.64 0.007 2.28 0.67 0.48 0.61 0.77 0.49 0.95 0.75 1.06 2.4E-03 0.99 2.1E-03 0.016 2.6E-03 0.014 0.44 0.013 0.46 0.46 Table(Continued) 1 nameCa-chloride Date Water Type
48 Table 5 (Continued). - Br - 3 NO - 3 HCO 2- 4 SO - Cl + K + Na 2+ Mg 2+ Ca S 34 δ Sr 86 Sr/ 87 B 11 ‰ ‰ mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L δ Alumot (km) Alumot Distance from Distance from
Table 1Table (Continued) name B2 Subgroup MikmanWadi MikmanWadi MikmanWadi MifshelMifshelMallaha 55.2 B3 Subgroup 55.2 MayallaAbu 55.3Uga Melecha MelechaUga 27/02/2001 Na-chlorideUga Melecha 09/04/2001 Na-chloride 58.8Uga Melecha 18/09/2000 Na-chloride 58.8Group C Date 72.5Zarqa River 70.3 Water Type 26.22Zarqa River 86.7 27/02/2001 RiverZarqa 86.7 Na-chloride 09/04/2001 0.70804 Na-chloride 27/02/2001 86.7 01/12/2001 Na-chloride 86.7 Mg-chloride 23/05/2000 07/08/2000 Mg-chloride Mg-chloride 29.47 23/04/2001 66.3 289 Mg-chloride 41.71 03/08/2001 66.3 0.70810 254 Mg-chloride 66.3 0.70797 248 547 5.6 18/09/2000 224 41.50 281 Mg-chloride 27/02/2001 59.8 273 740 09/04/2001 Mg-chloride 790 823 0.70804 Na-chloride 608 24.73 757 108.0 1344 -16.7 301 24.23 1045 3850 115.0 0.70871 375 27.5 280 306.0 329 1560 973 305 -17.1 262 0.70868 5900 280 984 350 1420 151 794 273 0.70857 301 3930 1300 9.5 1000 372 90.9 1200 649 343 180.0 5 10.0 100.0 184.0 2250 2930 158 353 240 1630 1025 150 2338 1515 254 237.0 290 100.0 930 2080 219 210 2000 5470 920 5 206 2250 335 5 138 1050 327 708 2980 259 1070 1010 890 317 100.0 36 106.0 64.9 237 96.0 1710 31 140 310 1720 25 1358 153 1150 2354 135 1140 1118 31 5 30 940 36 6 290 44 351 31 312 1 63 49 38 10 9 9 30
49 Table 5 (Continued). 4 /Cl Br/Cl Sr/Ca Ca/SO 4 TDS Na/Cl Q Mg/Cl Ca/Mg SO 2+ Sr 3+ B mg/L mg/L mg/L mM mM mM mM mM mM mM mM Alumot (km) Alumot Distance from Mikman MikmanWadi MikmanWadi MifshelMifshelMallahaSubgroup B3 55.2 MayallaAbu 55.2 55.3 MelechaUga 09/04/2001 MelechaUga 27/02/2001 18/09/2000 MelechaUga Na-chloride 58.8 Na-chloride MelechaUga Na-chloride 58.8Group C 72.5 1.5 70.3 27/02/2001 RiverZarqa 2.0 86.7 1.8 09/04/2001 RiverZarqa Na-chloride 86.7 RiverZarqa Na-chloride 11.0 01/12/2001 27/02/2001 86.7 Na-chloride 12.1 23/05/2000 9.8 4289 Mg-chloride 86.7 2.7 07/08/2000 4195 Mg-chloride 3847 2.5 1.20 23/04/2001 13.26 Mg-chloride 1.17 8.0 03/08/2001 66.3 15.9 1.03 Mg-chloride 0.31 2.5 66.3 14.5 0.31 15.0 Mg-chloride 5909 0.42 0.41 2.6 66.3 16.0 15508 5838 18/09/2000 0.39 2.4 1.23 0.45 13476 5.8 0.50 27/02/2001 1.01 Mg-chloride 2.0 1.22 0.54 0.32 5.8 09/04/2001 0.83 Mg-chloride 0.69 5274 0.45 0.54 0.29 5.6 Na-chloride 0.25 5278 0.55 0.60 2.3 0.67 5.7 2.2E-03 0.60 0.15 0.26 5406 2.5 2.0E-03 0.70 0.61 0.17 0.022 2.7E-03 0.61 5391 0.74 0.66 2.1 0.58 0.022 7.7 0.64 0.016 0.47 0.74 0.38 0.21 0.66 8.2 0.59 0.25 0.38 0.49 4245 0.22 1.5E-03 0.51 0.63 0.56 8.4 0.20 2.7E-03 4518 0.21 1.6E-03 0.026 0.80 0.53 0.22 3.6E-03 4796 0.009 0.15 0.025 0.95 0.53 0.61 0.32 0.009 0.15 0.96 0.53 6.1E-03 0.45 0.50 0.31 0.15 0.24 6.0E-03 0.64 0.009 0.45 0.15 0.18 5.7E-03 0.009 0.98 0.78 0.17 6.8E-03 0.009 0.69 0.81 0.30 0.009 0.75 0.74 0.25 3.4E-03 0.80 0.24 2.4E-03 0.010 2.3E-03 0.016 0.76 0.015 0.50 0.53 Table(Continued) 1 nameSubgroup B2 Date Water Type
50 2.2.2.2. The chemical composition of shallow boreholes in the southern section
All groundwater from the southern boreholes collected during the years 2004-2005 has a Ca-chloride composition (Q>1), with chloride concentrations in the range of
10,000 to 63,000 mg/L, low Na/Cl and SO4/Cl ratios (0.50-0.55 and ~0.03, respectively), and a high Br/Cl ratio (~6 x 10-3).
2.2.2.3. The chemical composition of springs and streams in the Jordan Valley
Spring and stream water samples were obtained from 2000 to 2004 along the lower Jordan River. These water samples represent a wide variety of water types and a wide range of salinities: from freshwater salinity with TDS of 300 mg/L to saline brines with TDS of up to 100,000 mg/L (Appendix I). Saline brines and diluted brines (i.e., saline groundwater that has a brine composition but with lower salinity) were detected in streams and springs in both the northern (10- 20 km south of Alumot Dam) and southern (70 to 100 km south of Alumot Dam) sections of the Jordan valley (Fig. 15). This water type is generally characterized by low Na/Cl (<0.7), high Q (>1), and Br/Cl (>2 x 10-3) ratios. These ratios changed spatially: in the northern part of the research area the Na/Cl ratio ranged from ~0.66 to ~0.70, in the southern part the range was ~0.46 to ~0.56. The Br/Cl ratio also ranged from ~5 x 10-3 in the north to ~6 x 10-3 in the south. The Mg/Cl ratio ranged between ~0.13 in the north and ~0.19 in the south. A similar spatial trend has been reported previously by Klein-Ben David et al. (2004), who based their interpretation on data from two disconnected (100 km distant) areas: saline springs in the vicinity of the Sea of Galilee in the north and the Dead Sea in the south. The 87Sr/86Sr ratios measured in the brines along the lower Jordan River (0.7078- 0.7080) are consistent with the findings of Stein et al. (1997) for the Ca-chloride brines near the Dead Sea. High δ11B values (up to 48‰) are also consistent with the Dead Sea brine (up to 57‰; Vengosh et al., 1991b). However, the δ34S values found for sulfate in the Jordan Valley brine-derived (+4‰ to +17‰) are lower than those reported in a previously study for Ca-chloride brines (> 20‰; Gavrieli et al., 2001).
51 In addition to the brine-derived, other types of low-saline groundwater were identified. The low-saline groundwater was classified into three different groups, each having unique chemical and isotopic characteristics, as well as different geographic locations (Fig. 17). The three different water groups are defined primarily according to their 87Sr/86Sr ratio values: low (Group A), intermediate (Group B), and high (Group C; Figs. 15, 17 and 18).
Hierarchy of the water types Group Group Group A B C
low 87Sr/86Sr Medium 87Sr/86Sr High 87Sr/86Sr Na-chloride Na-chloride
Subgroup Subgroup Subgroup B1 B2 B3 Na-chloride Na-chloride Mg-chloride negative δ34S positive δ34S negative δ34S
Fig. 17. Hierarchical division of the low-saline groundwater into three different groups based on their chemical and isotopic compositions and geographic locations.
52 10 Group B
8
6
4 Group A Number of analyses Number Group C 2
0 0.7068 0.7071 0.7074 0.7077 0.708 0.7083 0.7086 0.7089 87Sr/86Sr
Fig. 18. Histogram of 87Sr/86Sr ratios of the three different water groups: low (Group A), intermediate (Group B), and high (Group C) 87Sr/86Sr ratio.
Group A: is a Na-chloride freshwater group, and is characterized by a relatively low 87Sr/86Sr ratio (0.70693-0.70758; Table 5). This type of groundwater is found in the northern section in the Yarmouk River (Fig. 15). As mentioned before, the Adassiya Dam divides the Yarmouk River at base flow conditions (i.e., low flow rates) into a section with high-quality fresh water upstream of the dam and predominantly saline water downstream from the dam. The dam is opened only during rare large flood events, at which time the Yarmouk River flows and contributes high-quality fresh water to the lower Jordan River. The Yarmouk River water was sampled in three separate situations: (i) during a flood event (“flood”), (ii) during base-flow conditions upstream from the dam (“the fresh Yarmouk”), and (iii) during base-flow conditions downstream from the dam ("the saline Yarmouk"). Although these three distinct situations resulted in different chemical compositions, they are all classified as Group A, given their low 87Sr/86Sr ratios.
53 (1) The flood water at the Yarmouk River is characterized by low chloride concentration (~50 mg/L), low 87Sr/86Sr, Br/Cl, Sr/Ca and Q ratios (0.70693, ~1.7 x -3 -3 10 , 4 x 10 and 0.5-0.6, respectively) and high Na/Cl and SO4/Cl ratios (~1.2 and ~0.29, respectively; Table 5). (2) The upstream fresh water of the Yarmouk River is characterized by a slightly higher chloride concentration (up to 145 mg/L), 87Sr/86Sr, Br/Cl and Sr/Ca ratios (up to 0.70758, 3.6 x 10-3 and 7 x 10-3, respectively), Q ratio of 0.5-0.6 and lower Na/Cl 34 and SO4/Cl ratios (to ~1 and 0.22, respectively), relative to the floodwater. The δ S in the fresh Yarmouk water is +10‰ (Table 5). (3) The downstream saline Yarmouk water is characterized by high chloride 87 86 concentrations of ~1100 mg/L, and low Sr/ Sr, Na/Cl, SO4/Cl and Q ratios (0.70716-0.70719, ~0.9, 0.2-0.3 and 0.3, respectively; Table 5). In addition, the Br/Cl and Sr/Ca ratios are relatively high (4 x 10-3 and 7 x 10-3, respectively). The δ34S of the saline Yarmouk (-2‰) is twelve per mil depleted value relatively to the upstream fresh Yarmouk water (Table 5).
Group B: This saline water group is characterized by an intermediate 87Sr/86Sr ratio (0.70778-0.70820; Fig. 18). This group is further divided into three subgroups, based on their chemical and sulfur isotopic compositions and their geographical location in the Jordan Valley (Figs. 15 and 17 and Table 5). (1) Subgroup B1: a Na-chloride water type characterized by chloride concentrations below 600 mg/L, high Na/Cl and SO4/Cl ratios (up to 1.2 and 1.0, respectively), a low Q ratio (< 0.6) and Br/Cl ratio (2 to 3x10-3), negative δ34S (-5.4‰) and low δ11B values (21‰; Table 5). This fresh water was found in the northern section adjacent to Wadi Arab and Wadi Teibeh (~12-16 km south of Alumot Dam; Fig. 15). (2) Subgroup B2: a Na-chloride water type characterized by chloride concentrations of ~1500 mg/L, high nitrate content (~150 mg/L), high Na/Cl and SO4/Cl ratios (up to -3 1.3 and ~0.5, respectively) and low Br/Cl ratio (2 x 10 ). The Ca/SO4 and Ca/Mg ratios are lower than 1. The isotopic composition of this subgroup is characterized by positive δ34S (5.6‰) and relatively low δ11B values (<30‰; Table 5). This type of water was sampled mainly from the central-eastern bank of the Jordan Valley, 50 to 70 km downstream of Alumot Dam (Figs. 15 and 19). (3) Subgroup B3: a Mg-chloride water type characterized by chloride concentrations above 960 mg/L, a Na/Cl ratio of 0.6 to 0.8, a SO4/Cl ratio of 0.1 to 0.2 and Q ratio
54 lower than 0.65. The isotopic composition of this subgroup is characterized by 3 extreme negative δ 4S (-17‰) and high δ11B values (>40‰; Table 5). This type of water was observed only in the southern section, 70 to 100 km south of Alumot Dam (Figs. 15 and 19).
Group C: a Mg-chloride and Na-chloride saline water type (TDS ~4600 mg/L) -3 characterized by a Na/Cl ratio of ~0.9, Br/Cl ratio of 2 to 3 x 10 , a SO4/Cl ratio of 0.2 to 0.3 and a Q ratio lower than 0.61. The isotopic composition of this subgroup is characterized by a high 87Sr/86Sr ratio (0.70857-0.70871) and low δ11B values (24- 27‰; Table 5). This type of water was found in the southern section adjacent to the Zarqa River (~66 km south of Alumot Dam; Fig. 15).
1.4
Subgroup B2 B2 Ca-chloride B1 1.2
1 Na/Cl (M/M) 0.8 Subgroup B3
Ca-chloride Brine-derived 0.6
0.4 50 60 70 80 90 100 Distance from Alumot Dam (km)
Fig. 19. Variation of Na/Cl ratios (in M/M) versus distance from Alumot Dam as recorded in groundwater in the southern section. Note the different geographic locations of Subgroup B2 (mainly north of the 60-km), Subgroup B3 and the Ca- chloride brine-derived (65 km from Alumot Dam and southward).
55 2.2.3. Discussion
2.2.3.1. Overall distribution of saline brines in the Jordan Valley
Given that mixing of hypersaline brine and fresh water results in the formation of saline or even brackish groundwater with conservative ionic ratios that are identical to the saline end member, a “brine-derived” waters was defined to be groundwater with low Na/Cl and high Br/Cl ratios, regardless of its absolute salinity. The data presented here suggest that “brine-derived” groundwaters with a large range of salinity (1-63 g Cl/L) are found along the Jordan Valley, between the Sea of Galilee to the north, and the Dead Sea to the south (“central brine” in Fig. 15). These brine-derived was identified in both groundwater from shallow boreholes and in surface water sampled in springs and streams on both sides of the lower Jordan River.
The chemical composition of the brines is known to change spatially along the Rift Valley. Klein-Ben David et al. (2004) showed that the northern brine, adjacent to the Sea of Galilee, is characterized by Na/Cl ratios of 0.6 to 0.75 (Tiberias Hot Springs and Fuliya Spring, respectively). This ratio decreases southward to values of ~0.3 in saline springs adjacent to the Dead Sea (the southern brine; Klein-Ben David et al., 2004). The chemical characteristics of the shallow groundwater with the brine signature reported in this study mimic the general geographic trend observed in the hypersaline brines. The data presented here show a transition of Na/Cl ratios from 0.66-0.70 in the northern to 0.46-0.56 in the southern parts of the Jordan Valley. Likewise, a similar southward decrease of Mg/Cl ratio and an opposite southward increase in Br/Cl ratio were observed (Fig. 20).
The geographical geochemical trend observed in both hypersaline brines and shallow groundwater suggests that the pressurized deep brines (Rosenthal, 1987) rise to the surface and mix with shallow fresh groundwater along conductive zones in the Rift Valley, such as the faults along the Jordan Valley. This is supported by the work of Garfunkel and Ben-Avraham (1996), who showed intensive fracturing in the Jordan Valley. Structural maps (Krasheninnikov et al., 2005) point for a large amount of normal faults existing both in the valley’s margins as well as in the valley itself, adjacent to the river. These fractures may serve as preferential flow systems allowing rapid rise of brines from the deep sub-surface and their mixing with shallow
56 groundwater from the surrounding aquifers in the upper sections of the geological formation. In this respect, the brackish and saline shallow groundwater inherit their chemical character from geographically distributed parent brines that originated through different stages of evaporation and salt precipitation as suggested by Klein- Ben David et al. (2004).
0.012 0.8
0.01 0.7
0.6 0.008 Southern Br/Cl (M/M) Na/Cl (M/M) 0.5 Northern Central 0.006 Brines Brines Brines Central 0.4 0.004 Brines 0.3 Southern 0.002 Northern Brines Brines 0.2 -50 0 50 100 150 -50 0 50 100 150
3.5 0.3 Northern Southern 3 Brines Brines 0.25
2.5
0.2 Central 2 Brines Ca/Mg (M/M) Mg/Cl (M/M)Mg/Cl Northern 1.5 0.15 Brines
1 Central Brines Southern Brines 0.1 0.5
0 0.05 -50 0 50 100 150 -50 0 50 100 150 Distance from Alumot Dam (km) Distance from Alumot Dam (km)
Fig. 20. Br/Cl, Na/Cl, Ca/Mg and Mg/Cl ratios versus distance from Alumot Dam. The negative values on the x-axis (from -50 to 0 km) correspond to northern brines, which are sampled in a previous study (Klein-Ben David et al., 2004), near the northern part of the Sea of Galilee. The central brine-derived (from 0 to 100 km) correspond to boreholes and springs between the Sea of Galilee and the Dead Sea. The southern brines (from 100 to 150 km) were sampled in a previous study (Klein- Ben David et al., 2004) near the Dead Sea.
57 2.2.3.2. The origin of saline groundwater in the northern section of the central Jordan Valley
In the northern section of the Jordan Valley, two groundwater types without brine fingerprints were identified: the brackish to saline groundwater in the Yarmouk River basin (Group A) and groundwater from the eastern bank of the Jordan Valley, adjacent to Wadi Arab and Wadi Teibeh (12 to 16 km south of Alumot Dam; Group B1, Fig. 15). In addition, the brine fingerprints were identified in groundwater from shallow boreholes along the western bank of the Jordan Valley. Group A: Most of the flow of groundwater in the Yarmouk basin (Fig. 15) is in alkali basalts overlying chalks and marls of the Paleocene sequence (Belqa Group in Jordan, Mt. Scopus Group in Israel; Picard, 1965; Bender, 1968, 1974; Parker, 1970; Levitte et al., 1978; EXACT, 1998). The basalt in the vicinity of the Yarmouk River is a good aquifer, mainly due to its high porosity and permeability (EXACT, 1998). Most of the Yarmouk River's base flow is derived from this aquifer, mainly from the springs and surface inflows on the Syrian side of the river (EXACT, 1998; Fig. 15). The low 87Sr/86Sr (0.70693) and high Na/Cl (>1.1) ratios recorded in the flood-event water from the Yarmouk River suggest that the recharged water reacted with the alkali basalt rocks (Fig. 21). According to Stein et al. (1993), the alkali basalt rocks in this area have strontium isotopic composition lowers than 0.704. In contrast, the chemical composition of the saline groundwater of the saline Yarmouk water downstream of the Adassiya Dam is entirely different from that of the upstream water. The Yarmouk saline water exhibits a unique geochemical composition and is not similar to any of the other saline waters in the Jordan Valley. The data shows that the + 2- 3+ contents of different ions (Na , SO4 , and B ) and isotopic ratios of oxygen and nitrogen are positively correlated with chloride (Figs. 22 and 23).
58 1.2
Flood
1.1 Fresh Yarmouk
1 Saline Yarmouk
0.9 Na/Cl (M/M)
0.8
0.7 0.001 0.002 0.003 0.004 0.005 0.006 Br/Cl (M/M)
Fig. 21. Na/Cl versus Br/Cl ratios in the Yarmouk River water in three distinct situations: during a flood event, as fresh Yarmouk water upstream of the Adassiya Dam and as saline Yarmouk water downstream of the dam. Note the difference between the flood water and the saline water, not only with respect to the ion-ratio trend but also in the different 87Sr/86Sr ratio.
These chemical and isotopic fingerprints are not consistent with the expected composition upon dilution of brines (e.g., Tiberias Hot Springs; Starinsky, 1974). The results of a mass-balance calculation between the fresh Yarmouk and the brine (Tiberias Hot Springs) components indicate that the Na/Cl and Br/Cl ratios in the saline Yarmouk are too high and low, respectively, to account for possible dilution of brine, given the chloride content of the saline Yarmouk water. For example, mixing between two end members was calculated: (1) fresh flood Yarmouk River (Cl- = 50 mg/L, Na/Cl = 1.11 and Br/Cl = 1.8 x 10-3); and (2) the Tiberias Hot Springs (Cl- = 18,400 mg/L, Na/Cl = 0.59 and Br/Cl = 5.8 x 10-3; Starinsky, 1974). Mixing these two components for the salinity measured in the saline Yarmouk River (Cl- ~ 1300 mg/L) would produce saline water with a Na/Cl ratio of ~0.6 and Br/Cl ratio of ~5.6 x 10-3. These values are completely different from the ratios measured at the saline Yarmouk water (~0.8 and 4 x 10-3, respectively).
59 350 1200 Evaporation 300 Evaporation line 1000 line 250 800 Saline 200 Saline Yarmouk 600 (mg/L) 150 4 Yarmouk Mg (mg/L) Mg SO 400 100
50 Fresh Yarmouk 200 Fresh Yarmouk Yarmouk- Flood Yarmouk- Flood 0 0 0 500 1000 1500 2000 0 500 1000 1500 2000 Cl (mg/L) Cl (mg/L)
1200 350 Evaporation Evaporation 300 1000 line line 250 800 Saline 200 600 Yarmouk Saline 150
Ca (mg/L) Yarmouk Na (mg/L) Na 400 100 Fresh Yarmouk 200 Fresh Yarmouk 50 Yarmouk- Flood Yarmouk- Flood 0 0 0 500 1000 1500 2000 0 500 1000 1500 2000 Cl (mg/L) Cl (mg/L)
2+ 2- + 2+ - Fig. 22. Mg , SO4 , Na and Ca concentration versus Cl concentration (in mg/L) of the Yarmouk River water in three separate situations: (i) during a flood event (“Yarmouk-Flood”), (ii) under base-flow conditions upstream of the dam (“Fresh Yarmouk”), and (iii) under base-flow conditions downstream of the dam ("Saline Yarmouk").The continuous line represents the calculated evaporation trend in the 2+ 2- + - saline Yarmouk water. Note that while most major elements (Mg , SO4 , Na and Cl ) are conservatively concentrated during the evaporation process, Ca2+ is significantly reduced probably due to precipitation of calcium carbonate.
The high concentration of boron (up to 5 mg/L) and the high δ15N (11 to 17‰; Fig. 23) values in the saline Yarmouk suggest that it is derived from anthropogenic sources composed of a mixture of animal waste effluents, agricultural return flows, and domestic waste waters. Segal-Rozenhaimer et al. (2004) showed that nitrate content in the lower Jordan River is continuously increased by input from nitrate-rich groundwater with high δ15N values that also characterizes the Yarmouk saline groundwater. Likewise, man-made effluents (e.g., sewage or agricultural return flows) have typically high boron concentrations (Vengosh, 2003).
60
The 87Sr/86Sr ratio of the saline Yarmouk is lower than the 87Sr/86Sr ratio of the upstream fresh Yarmouk (~0.70718 and 0.70755, respectively) and the 87Sr/86Sr ratios observed in the Yarmouk River during the flood event (0.70693-0.70714). Bullen et al. (1996) showed that the 87Sr/86Sr ratio in water depends on the degree of chemical equilibrium with the local rocks. Given that most of the local permeable rocks around the Yarmouk River are basaltic, it has been speculated that the fresh Yarmouk water with low 87Sr/86Sr ratios is used for irrigation in the northern Jordan Valley and being returned back to the Yarmouk channel downstream of the dam as agricultural effluents, forming the saline Yarmouk. Consequently, the agricultural return flow discharges to the Yarmouk channel through basaltic pebbles and therefore intensify the water-rock interactions with the basaltic pebbles, resulting in a lower 87Sr/86Sr ratio relative to the original fresh Yarmouk water. Irrigation by the fresh Yarmouk water causes recycling of salts and accumulation in the shallow drainage water. The positive correlation of the different ions with chloride, coupled with the high δ18O signal (range of -3.6 to -2.5‰; Fig. 23) indicate that the high salinity is a product of extensive evaporation of the shallow drainage waters. While most of the major elements are conservatively concentrated during the - 2+ evaporation process, HCO3 and Ca are significantly reduced, probably due to precipitation of calcium carbonate in the soil (Fig. 22). PHREEQC software was used (Parkhurst and Appelo, 1999) to model the saturation state of pertinent minerals and find that the saline Yarmouk is often supersaturated with respect to calcite (SI in the range of 0.8-1.3) whereas the fresh Yarmouk water is under saturated (SI = 0.06).
61 -2.6 18
17 -2.8 Curve fit 2 16 R = 0.913 Curve fit
2 (‰) -3 R = 0.803 15 NO3 O (‰) N 18 14 δ -3.2 15 δ Saline 13 Yarmouk Saline -3.4 12 Fresh Yarmouk Yarmouk -3.6 11 0 200 400 600 800 1000 1200 1400 1600 0 200 400 600 800 1000 1200 1400 1600 Cl (mg/L) Cl (mg/L)
Fig. 23. δ18O and δ15N values versus Cl- concentration (in mg/L) of the Yarmouk River upstream ("Fresh Yarmouk") and downstream ("Saline Yarmouk") to the dam. Note the isotopic positive correlations with chloride in the saline Yarmouk water.
Subgroup B1: The second water type identified in the northern section of the Jordan Valley is a Na-chloride water type (subgroup B1). This type of water was found on the eastern bank of the Jordan Valley, adjacent to Wadi Arab and Wadi Teibeh, 12 to 16 km south of Alumot Dam (Fig. 15). This water group is relatively fresh, with chloride concentrations below 600 mg/L. The sulfate concentration (~1400 mg/L) in subgroup B1 is higher than the chloride 34 concentration. The very high SO4/Cl ratio (0.6-1.0) and negative δ S values (-5.4‰) most likely reflects oxidation of sulfide minerals to sulfate. The negative δ34S values in subgroup B1 eliminate other sulfate source like gypsum dissolution, which would 34 have produced positive δ S values. Ca/SO4 and Sr/Ca ratios provide additional evidence for the argument that gypsum dissolution is not the source of sulfate in the sulfate-rich groundwater. Dissolution of gypsum would produce water with Ca/SO4
~1 and a low Sr/Ca ratio, yet the groundwater of this group has Ca/SO4 ~0.5 and high Sr/Ca ratios (~0.01). It was concluded that the high sulfate concentration and negative δ34S values reflect oxidation of sulfide minerals (e.g. pyrite) as the main process that contributing sulfate to the water. This argument is also supported by geological evidence: the sulfate-rich water type (subgroup B1) is identified within the chalk-marl rocks of the Belqa Group (B1-B3; Upper Cretaceous to Eocene; Bender, 1974), which are known to contain pyrite in central and northern Jordan (Pufahl et al., 2003).
62 The low salinity of subgroup B1, along with the high Na/Cl ratio and low Q value (Table 5) indicate that the water composition of subgroup B1 is not influenced by brine mixing.
Brine contribution to shallow groundwater in the northern part of the lower Jordan Valley: The chemical composition of the shallow groundwater from the Northern boreholes (Fig. 1) shows both temporal and spatial variation in both solutes concentration and ionic ratios (Table 1). However, the data presented here shows that the Na/Cl and SO4/Cl ratios decrease with increasing salinity. These relationships suggest that brines with typical geochemical characteristics are affecting the overall salinity and chemical composition of the shallow groundwater, particularly in the vicinity of Boreholes 4 and 5. Mixing calculations between a brine (represented by the Tiberias Hot Springs composition) and a fresh water component (as sampled in Borehole 1) reveals a brine contribution of up to ~30% of the solute composition (at Borehole 4; Fig. 3). In other wells, (e.g., Boreholes 1 and 2), however, the effect of the brines is negligible. Moreover, the data show that a simplistic mixing model cannot always explain the water composition of the shallow groundwater. In some wells we observed data points that offset from the theoretical mixing line between brine and fresh water. Thus, additional processes such as water-rock interactions, oxidation-reduction processes, and mixing with other water bodies also control the chemical composition of the shallow groundwater. For example, groundwater from Borehole 3, which is located very close to the Jordan River, showed the highest diversion from the theoretical mixing line. Given that the water level and chemical composition (e.g., Na/Cl=0.78,
SO4/Cl ~0.1) in this well was found to be similar to those in the adjacent Jordan River (see in Farber et al., 2004), it is most likely that the chemical composition of the groundwater is influenced by lateral flow of the saline Jordan River.
2.2.3.3. Brine contribution to saline groundwater in the central and southern Jordan Valley
Two groups of water with similar 87Sr/86Sr ratios (0.70778-0.70820) were observed in the central and southern Jordan Valley, the Na-chloride (subgroup B2) and the Mg- chloride (subgroup B3; Table 5) water types. Subgroup B2 was identified mainly in
63 the central part of the Jordan Valley (50-70 km south of Alumot Dam), whereas subgroup B3 was found in its southern part (70-100 km south of Alumot Dam; Fig. 15). The brine contribution to each of these subgroups is discussed below.
2.2.3.3.1. Subgroup B2: Na-chloride water type
The saline water of subgroup B2 is characterized by chloride concentrations of ~1500 mg/L, high nitrate content (~150 mg/L), a high SO4/Cl ratio (~0.5) and a high Na/Cl ratio (up to 1.3; Table 5). The isotopic composition of this group is characterized by positive δ34S (+5.6‰) and relatively low δ11B (~30‰) values (Table 5). The high nitrate concentration indicates an anthropogenic contribution for this water. Given that this type of water is found only on the eastern side of the Jordan Valley, it was postulated that the higher agricultural activity along the eastern side of the Jordan Valley results in formation of a large volume of agricultural effluents that contribute to this type of groundwater. The geological strata in this part of the Jordan Valley are composed of the Samra and Lisan formations, which are part of the Dead Sea Group (Picard, 1943; Bentor and Vroman, 1960; Bentor, 1961; Begin, 1975). The Samra formation is a clastic lacustrine unit that includes evaporite layers (i.e., authigenic aragonite or calcite, gypsum and halite), sand, marl and conglomerate (Picard, 1943; Stein et al., 2005). The overlying Lisan formation includes chemically precipitated aragonite, gypsum and traces of halite, and detrital sediments composed of calcite, quartz, dolomite and clay minerals (Begin et al., 1974). Water flow through the halite and gypsum units would increase the + - 2+ 2- water's Na and Cl (due to halite dissolution), and the Ca and SO4 concentrations (due to gypsum dissolution). In sum, the saline groundwater of this group can be derived from three sources: - agricultural return flow (high NO3 ), evaporate dissolution (high Na/Cl and SO4/Cl ratios, relatively low δ11B), and central brine contribution (high Br/Cl ratios). The relatively low Br/Cl ratio in water subgroup B2 rules out any third option; the brine contribution. + - 2- The high concentrations of Na , Cl , and SO4 indicate that water flow through the Lisan and Samra formations dissolved the halite and gypsum salts. In some of the water samples, the Na/Cl ratios were higher than 1 and in all of the samples, the Ca/SO4 ratios were lower than 1. The relative excess of Na+ and deficiency in Ca2+ may suggest further modification by an ion-exchange process that typically occurs in clay-rich
64 sediments, such as those of the Samra and Lisan formations. During this process, Ca2+ in the solution is exchanged with Na+ in the sediments. The ion-exchange process could explain the excesses of Na+ (Na/Cl > 1) and Mg2+ (Ca/Mg < 1) and the relative 2+ deficiency of Ca (Ca/SO4<1). Likewise, the relatively low δ11B values (~30‰) also indicate that gypsum dissolution is the predominant process controlling the water composition. Vengosh et al. (1992) showed that during brine evolution and salt crystallization, the residual brine is enriched in 11B, whereas the salts become depleted due to selective uptake of 10B by the precipitates. Hence, the dissolution of the Lisan gypsum was expected to result in sulfate-rich water with relatively low d11B values. Assuming that the Br/Cl ratio subgroup B2 (2.7 x 10-3) reflects remnants of evaporated seawater, the Br/Cl ratio corresponds to 20-fold evaporated seawater with Na/Cl ratio of ~0.7 (data from McCaffrey et al., 1987). However, the mass-balance calculations show that the relative excess of sodium (8-17 meq/L) is not balanced by calcium depletion (13-30 meq/L), inferring that the Br/Cl ratio (2.7 x 10-3) is not an indicator for brine evolution but rather reflects the mixture of solutes with both high (brines) and low (halite dissolution) Br/Cl ratios.
2.2.3.3.2. Subgroup B3: Mg-chloride water type
The subgroup B3 Mg-chloride saline water is characterized by chloride concentrations of up to ~1000 mg/L, relatively low SO4/Cl ratios in the range of 0.1 to 0.2, a low Na/Cl ratio of <0.8, and low Q values (< 0.65). The isotopic composition in this subgroup is similar to that of the typical Ca-chloride Rift Valley brines with respect to the δ11B (>40‰) and 87Sr/86Sr (~0.7080) values. However, the δ34S of the brackish groundwater (-17‰) is almost forty per mil depleted value relatively to typical Ca- chloride brines (>20‰; Gavrieli et al., 2001; Table 5). Likewise, the low Q values differ from the typical Ca-chloride brines with Q > 1. The Mg-chloride water type of subgroup B3 flows in the sediments of the Samra and Lisan formations (Figs. 15 and 16). The Samra and Lisan sediments have similar strontium isotope ratios but different sulfur isotope ratios than the typical Rift Valley brine. The 87Sr/86Sr ratios measured in the Samra and Lisan formations range from 0.70805 to 0.70838 and 0.708026 to 0.708075, respectively (Raab et al., 1997; Stein et al., 1997). According to Raab et al. (1997) and Stein et al. (2000), the δ34S values of these sediments fall within the narrow range of 18 to 24‰, whereas the δ34S values
65 of subgroup B3 are negative (-17‰; Table 5). Overall, conflicting results were obtained: on the one hand, the geochemical parameters reflect simple leaching of the local sediments (e.g., 87Sr/86Sr ratios); on the other, the chemical composition of this type of water resembles, but is not identical to the composition of the Rift Valley brines (e.g., low Na/Cl ratios). Moreover, the depleted δ34S values are not found in both the local sediments and the Rift Valley brines. It was proposed that the Mg-chloride water type was generated by a mixing process between the Ca-chloride brine and a Na-chloride water type (subgroup B2; Fig. 24), coupled with sulfide oxidation or dissolution of sulfate minerals with negative δ34S values as the source for the 34S-depleted sulfate. The suggested Na-chloride end member is located north (upstream) of subgroup B3, whereas the Ca-chloride end member is found in the central and southern parts of the rift. Figure 24 presents' possible mixing combinations between the Ca-chloride brine- derived and the water of subgroup B2 for different ion ratios (Na/Cl, SO4/Cl and Q ratios). According to the mixing relationships, it can be estimated that subgroup B3 reflects a mixing product of 7 to 20% contribution of the Ca-chloride brine component. While the chemical variations match possible mixing with the Ca-chloride brines (with positive sulfur isotope values), the negative δ34S values (~ -17‰; Fig. 25) in the Mg-chloride water of subgroup B3 are not consistent with this mixing hypothesis. Thus, it can be argued that the isotopic shift is due to water-rock interactions with disseminated (secondary) gypsum within the aragonites of the Lisan or Samra formations with negative δ34S values (as low as -26‰; Gavrieli et al., 1998; Torfstein et al., 2005).
66
100% 30% 20% 10% 0% Ca-chloride brine- derived 2
Borehole G-1
1.5 ]; in M/M) 3
+HCO Subgroup
4 1 B3
Subgroup
Q (Ca/[SO B2 0.5
Wadi Mikman
0.4 0.6 0.8 1 1.2 1.4 Na/Cl (M/M)
100% 30% 20% 10% 0% 1 Wadi Mikman
Subgroup B2
0.1 Subgroup
/Cl (M/M) /Cl B3 4 SO Borehole G-1
Ca-chloride Brine-derived
0.01 0.4 0.5 0.6 0.7 0.8 0.9 1 Na/Cl (M/M)
Fig. 24. (A) Q (Ca/[SO4+HCO3]) and (B) SO4/Cl versus the Na/Cl ratio (in M/M) of a calculated mixing line in the southern groundwater (50 to 100 km downstream of Alumot Dam). The measured data of subgroups B2 and B3 and the Ca-chloride brine- derived are compared to calculated mixing lines between the fresh component of subgroup B2 and the saline component of the Ca-chloride brine-derived (as sampled in the boreholes and springs along the Jordan Valley). Note that subgroup B3's composition is determined by the mixing relationship between the subgroup B2 component as measured in Wadi Mikman (~90%) and the brine-derived component as measured in the southern borehole G-1 (~10%; Table 5).
67
20
15 Ca-chloride Brine-derived 10 Subgroup B2 5
S (‰) 0 34 δ -5
-10
-15 Subgroup B3 -20 0 0.05 0.1 0.15 0.2 0.25
SO4/Cl (M/M)
Fig. 25. Sulfur isotope composition (‰) versus SO4/Cl ratio (M/M) in the southern groundwater (50 to 100 km downstream of Alumot Dam). Note the negative values of the sulfur isotope ratio (~ -17‰) in the subgroup B3 water which are suggested to be the result of water-rock interactions with disseminated (secondary) gypsum.
2.2.3.4. Geothermal water in the Zarqa area—group C
Groundwater with the highest 87Sr/86Sr ratios is found in the foothills and highlands area in the vicinity of the Zarqa River (Fig. 15). The groundwater in this area is associated with the outcrops of Triassic, Jurassic and Lower Cretaceous rocks and is discharge from the Nubian Sandstone aquifers to the Jordan Valley (Salameh, 2002). The saline water (TDS ~ 4600 mg/L) in the vicinity of the Zarqa River is characterized by high 87Sr/86Sr ratios (0.70857-0.70871) and low δ11B values (24- 27‰; Table 5). The high strontium isotopic ratios are typical for the weathering of feldspar minerals, which are abundant in the arkosic sandstones of the Kurnub Group (Nubian sandstone) aquifer. The Kurnub sandstone is an erosion product of granitic rocks that contain radiogenic 87Sr, and it can therefore be assumed that groundwater
68 flowing through these sediments would acquire high 87Sr/86Sr ratios (e.g., Fritz et al., 1987; Austin, 1992; Mook, 2000). Figure 26 shows an increase in the 87Sr/86Sr ratios along the lower Jordan River. The maximum 87Sr/86Sr values were measured in the Zarqa River itself, which drains the central zone of the Kurnub units. The high Na/Cl (up to 0.96) and SO4/Cl (up to 0.3) ratios, and the lower Br/Cl (2-3 x 10-3) ratios also indicate that this type of water is not affected by mixing with the central brine.
Kurnub North
Lower Jordan River Zarqa R. Group Sea of of Sea Galilee Sea Dead Dead
0 10 20 30 40 50 60 70 80 90 100
0.7088
0.7087
0.7086
Sr 0.7085 86
Sr/ 0.7084 87
0.7083
0.7082
0.7081 56 58 60 62 64 66 68 70 72 Distance from Alumot Dam (km) Fig. 26. Strontium isotopic ratio versus distance from Alumot Dam (km) in groundwater adjacent to Zarqa River and Kurnub Group exposure (56 to 72 km downstream of Alumot Dam). Note the increase in the 87Sr/86Sr ratio of groundwater near the exposed Kurnub Group (Nubian sandstone) aquifer.
69 2.2.4. Summary and conclusions This section presents the geochemistry of the water resources in the central Jordan Valley between the Sea of Galilee and the Dead Sea, and evaluates the origins of the shallow-water resources with respect to the Rift Valley brines. The brine fingerprints were observed along both the eastern and western banks of the lower Jordan River. A geographical-chemical trend was observed in the Na/Cl and Br/Cl ratios that are consistent with a larger scale south-to-north shift in ionic ratios of brines (Klein-Ben David et al., 2004). These findings provide new information for this part of the Jordan Valley that previously had only scarce information. The chemical and isotopic fingerprints of the Ca-chloride Rift Valley brines were detected in shallow groundwater and surface water in the Jordan Valley. The brines were found to play a significant role in affecting the chemical composition and quality of different groundwater bodies between the Sea of Galilee and the Dead Sea. In addition, the hydrogeological investigations revealed layers of high conductivity (e.g., conglomerate, sandstone) within otherwise low-permeability units in which the saline water is flowing and mixing with different types of water that flow into the Rift Valley. Overall, it was shown that in addition to the contribution of the brines, water- rock interactions, evaporation and anthropogenic return flow often affect the groundwater chemical composition in the central Jordan valley.
70
2.3. Management scenarios for the Jordan River salinity crisis
2.3.1. Introduction Management of cross-boundary rivers requires full cooperation between the riparian states. In many cases, the upstream country controls the river’s flow rate (e.g., Euphrates, Nile, Colorado, Rio Grande, Danube and Mekong) and thus many conflicts arise due to uneven distribution or unilateral changes in water utilization. In addition to water-quantity distribution, water quality has become an important factor determining the ability to utilize river water. This is due to the fact that the quality of many international rivers has deteriorated significantly over the last decades (Shmueli, 1999). The problems involved in applying international treaties for international rivers include heterogeneities in drinking-water standards (e.g., the Danube River; Linnerooth, 1990), water laws, and management systems (e.g., the Rio Grande River; Schmandt, 2002) among the riparian states. The joint management of an international river requires a comprehensive scientific understanding of the processes controlling the degradation of the river’s quality. In this chapter, the lower Jordan River system is used to demonstrate that scientific understanding of the hydrological system is the key for sustainable joint management among riparian states. As already mentioned, the lower Jordan River marks the international border between Israel on the west and the Hashemite Kingdom of Jordan on the east. Decades of diversion of upstream good-quality water and direct dumping of saline water and wastewater have severely damaged the river’s ecological system. The salinity of the lower Jordan River has risen significantly (up to 5400 mg Cl/L in the summer of 2001), endangering its capacity to supply water, even to saline-resistant crops such as palms, which are one of the main agricultural products of the Jordan Valley. At the same time, the Jordan River is an important component of the Peace Treaty between Israel and Jordan (Israel-Jordan Peace Treaty, Annex II, 1994). The water issue is an essential aspect of the treaty and received the same level of attention as security and territorial issues. Concerning the Jordan River, it was agreed that (1) “Jordan is entitled to an annual quantity equivalent to that of Israel, provided, however, that Jordan’s use will not harm the quantity or quality of Israeli uses” (Annex II, article 2); (2) “Saline springs currently diverted to the Jordan River are earmarked for
71 desalinization” (Annex II, article 3); and (3) “Israel and Jordan will each prohibit the disposal of municipal and industrial wastewater into the course of the Yarmouk River or the Jordan River before they are treated to standards allowing their unrestricted agricultural use” (Annex II, article 3). Although the peace treaty was signed a decade ago, none of these items have been implemented. However, future development in the region will require dealing with them. The complexity of the hydrological system and the severe degradation of the water quality make future management schemes even more difficult to design. Based on our understanding of the hydrological and geochemical system of the lower Jordan River, it is expecting that implementation of the treaty is likely to lead to further degradation in the river water's quantity and quality. The relationships between surface inflows and groundwater discharge to the river were used to quantify the salt budget and hence the salinity of the lower Jordan River. Different management scenarios related to the implementation of the peace treaty were then simulated to predict the river's consequent flow rate and salinity. In sections 2.1 and 2.2, the lower Jordan River was divided into three sections according to chemical composition (Fig. 27): (1) a northern section (up to 20 km downstream of Alumot Dam) in which the initial high chloride concentrations decrease and sulfate concentrations increase downstream; (2) a central section (20-60 km downstream of the dam) in which the variation in chemical composition is less significant and mimics the upstream composition; and (3) a southern section (60-100 km) in which the chloride and sulfate concentrations increase downstream (Fig. 27). In this chapter, the northern and central sections are combined, and a new division is referred to (Fig. 28): a northern segment (“Segment One”, up to 66 km downstream of Alumot Dam) and a southern segment (“Segment Two”; from 66 to 100 km downstream to Alumot Dam). The distance of 66 km was chosen as the limit between segments One and Two because this is the point in the river at which significant salinization processes begin (Fig. 3A, Chapter 2.1).
72 2800 1400 2800 1400 2600 Mar 2000 1200 2600 Mar 2001 1200 2400 1000 2400 1000 2200 2200 800 800 2000 2000 (mg/L) 600 600 4 Cl (mg/L) 1800 1800
400 SO 1600 1600 400 1400 200 1400 200
020406080100 0 20 40 60 80 100
2800 1400 2800 1400 2600 Aug 2000 1200 2600 Jun 2001 1200 2400 1000 2400 1000 2200 2200 800 800 2000 2000 (mg/L) 600 600 4
Cl (mg/L) 1800 1800
400 SO 1600 1600 400 1400 200 1400 200
0 20406080100 0 20 40 60 80 100
2800 1400 6000 2000 2600 Feb 2001 1200 5500 Aug 2001 5000 2400 1000 1500 2200 4500 800 4000 (mg/L) 2000 1000 600 3500 4
Cl (mg/L) 1800 3000 1600 400 500 SO 2500 200 1400 2000 0 20406080100 0 20406080100 Aerial distance from origin (Alumot Dam; in km) Legend Cl
SO4
Fig. 27. The variation of chloride and sulfate contents (in mg/L) with aerial distance along the lower Jordan River as recorded in separate months. Note that the y-axis range was increased for the August 2001 results to include the high salinity peak.
73 Saline Waste carrier Sea of Water Galilee Alumot Dam
0 W. Yavniel Yarmouk Adassiya Dam SEGMENT W. Tabor ONE 10 W. Arab
Neve Ur N Syria W. Telbeh Upper Sea of Jordan River Jordan River Y W. Harod ar 20 Galilee mo W. Ziglab uk W. Nimrod W. Abu Ziad Israel Shif’a Station
Palestinian Authority Jordan 60 Zarzir Zarqa
Faraa /Tirza River Jordan Lower Adam Bridge Aqraa Dead Sea El Achmar 70 W. Mallaha Distance from Alumot Dam (km) 80 Melecha W. Shueib & Uga SEGMENT 25 km TWO 90 .
Abdalla Bridge 100
Dead Sea
Fig. 28. Schematic map of the lower Jordan River.
2.3.2. Methodology As shown in section 2.1 and by Holtzman et al. (2005), the water balance of the lower Jordan River is controlled by the groundwater flow along different parts of it. Hence, a mass-balance equation of the water in the river can be given as:
n n fi = in + sw + gw Q Q ∑ Qi ∑ Qi (2) i=1 i=1 where Qfi is the total water discharge (L/s) at the end point of an investigated section,
n in sw Q is the water discharge at the initial point of an investigated section, ∑ Qi is the i=1
n gw total discharge of several (n) surface-water sources along the section, and ∑ Qi is i=1 the total discharge of several (n) groundwater sources along the section. For the solute mass balance, the conservation of mass of that solute was added:
74 n n fi fi = in in + sw sw + gw gw C Q C Q ∑Ci Qi ∑Ci Qi (3) i=1 i=1 According to equations (2) and (3), if one quantifies the groundwater flow into the river, one can calculate the salinity of the river at any point along it, by following:
n n in in + sw sw + gw gw C Q ∑ Ci Qi ∑ Ci Qi fi = i=1 i=1 C n n (4) in + sw + gw Q ∑ Qi ∑ Qi i=1 i=1 In the previous sections and according to Holtzman et al. (2005), the contribution of the surface water and its solutes to the river water was found to be negligible. Therefore, equation (4) can be reduced to the following form:
n in in + gw gw C Q ∑ Ci Qi fi = i=1 C n (5) in + gw Q ∑ Qi i=1 If, however, the flow rates are unknown, it is still possible to determine the relative mass contribution of the groundwater sources to the river. In a system where the groundwater contribution is homogeneous (i.e., there is a single groundwater source), the solute mass balance will be: C fi = C gw f gw + C in (1 − f gw ) (6) and the relative contribution, f gw, is defined as: ( C fi − C in ) f gw = (7) ( C gw − C in )
In the two segments of the lower Jordan River, the groundwater flow and the salt mass balance in the river were quantified under the current hydrological conditions. In the northern segment of the river, the solute mass balance was used to determine the relative contribution of the groundwater salt flux (equations 6 and 7). In the southern segment, actual flow measurements and water quality in the river were used to quantify the relationships between river water and groundwater, and possible changes in river salinity upon changing the parameters of river flow (equation 5).
75 2.3.3. Results and discussion
2.3.3.1. The northern segment of the lower Jordan River
2.3.3.1.1. Current situation
The northern segment of the lower Jordan River extends from Alumot Dam to Adam Bridge (Segment One—the upper 66 km; Fig. 28). The downstream side of the Alumot Dam constitutes the headwaters of the lower Jordan River. The dam separates the Sea of Galilee from these headwaters (Fig. 29). As already mentioned, the base flow of the river begins at Alumot Dam and is composed of two principal components (Fig. 29): (1) saline springs that emerge along the western shore of the Sea of Galilee and are diverted to the lower Jordan River via the so-called “Saline Water Carrier” (SWC). This carrier is an artificial conduit, built to lower the natural salinity of the Sea of Galilee by draining the waters of several saline springs along its western shore to Alumot Dam. The saline water in the SWC is derived primarily from the Tabgha Springs and Tiberias Hot Springs (THS); (2) sewage effluents derived from the municipal sewage water of Tiberias (drained directly into the SWC) and from regional agricultural and municipal sewage that is treated and drained through a separate pipeline (“Bitaniya” sewage; Fig. 29). The current average discharge of this combined base flow is approximately 30 MCM/year (Holtzman, 2003; Fig. 29). Mixing between these two sources occurs at the initial point of the lower Jordan River, downstream of Alumot Dam.
76 Saline Water Carrier
Tabgha 15 MCM/y
Sea of Galilee
Sewage Tiberias 3.5 MCM/y Hot Spring 1.5 MCM/y
Bitaniya Sewage ~20 MCM/y ~10 MCM/y Deganiya Dam
Alumot Dam
Lower Jordan River
Fig. 29. Schematic map and annual discharge (MCM/year) of Bitaniya sewage and the Saline Water Carrier (data information from El-Ezra, M., 2004. Mekorot, Jordan Area, personal communication).
The relative proportions of salt contents from the respective sources contributing to the river water at the beginning of the lower Jordan River were determined using mixing equations 6 and 7. Whereas the annual discharge of Tabgha Springs is larger by an order of magnitude than that of THS (15 MCM/year versus 1.5 MCM/year), the salinity of THS (Cl- = 18 g/L) is much higher (Tabgha Springs, Cl- = 3 g/L). Consequently, the chemical composition of the mixed water in the SWC is controlled mainly by the higher saline component of the THS, although some contribution of Tabgha Springs is also identified (Fig. 30A). Given that the saline THS dominates the chemical composition of the water at the initial point of the lower Jordan River, the salt contribution of the Tabgha Springs cannot be evaluated by using the chemical variations, and thus is neglected in the following calculations.
77 1.0 A Sewage
0.9
0.8 Tabgha
Na/Cl (M/M) 0.7 Saline Water Carrier
0.6 Tiberias Hot Springs
0.5 0 0.0005 0.0010 0.0015 0.0020 0.0025
0.09 B 0.08 Sewage 0.07
0.06
0.05 /Cl (M/M) /Cl 4 0.04
SO Tabgha 0.03 Saline Water Carrier
0.02 Tiberias Hot Springs 0.01 0 0.0005 0.0010 0.0015 0.0020 0.0025 1/Cl (L/mg)
Fig. 30. Na/Cl (A) and SO4/Cl (B) versus 1/Cl (L/mg) of the saline water springs (i.e. Tabgha and Tiberias Hot Springs), sewage water (as sampled at Bitaniya) and the Saline Water Carrier (SWC; as sampled below the Alumot Dam). Note that the salt content of the SWC is controlled by the chemical composition of Tiberias Hot Springs and not Tabgha Springs.
78 A salt mass balance (equation 6) between the chloride contents in the sewage and the saline (THS) components reveals that the saline water contribution to the initial base flow of the lower Jordan River varies from 6% to 10% of the total salt budget (Table 6). Here the “f” value (equation 7) refers to the relative salt contribution of the saline component. The variations of other dissolved constituents normalized to chloride
(Na/Cl, SO4/Cl, Ca/Mg, and Ca/SO4 molar ratios; Fig. 31) reflect similar mixing relationships between the sewage and saline components (i.e., about 10% of the salt budget of the initial river at Alumot Dam is derived from the saline component).
Table 6. Calculation of the mixing proportions (f) between the saline component (as sampled at Tiberias Hot Springs) and sewage component (average of samples from Bitaniya sewage) that composed the initial base flow of the lower Jordan River at Alumot Dam (in separate months). Calculations were made for different major elements.
Name Date Ca Mg Na Cl SO4 Tiberias Hot Springs (THS) Moise et al., 2000 mg/L 3523 680 7042 18081 827 Bitaniya Sewage average mg/L 91 61 271 451 93 Alumot Dam mg/L 347 98 850 1860 150 THSFeb 1 2001 f (%) 7 6 9 8 8 Bitaniya Sewage f (%) 93 94 91 92 92 Alumot Dam mg/L 359 97 855 1970 150 THSMar 1 2001 f (%) 8 6 9 9 8 Bitaniya Sewage f (%) 92 94 91 91 92 Alumot Dam mg/L 378 105 930 2070 160 THSApr 1 2001 f (%) 8 7 10 9 9 Bitaniya Sewage f (%) 92 93 90 91 91 Alumot Dam mg/L 363 104 950 2040 158 THSMay 1 2001 f (%) 8 7 10 9 9 Bitaniya Sewage f (%) 92 93 90 91 91
The chemical composition of the initial base flow of the lower Jordan River changes along the first 22 km downstream of Alumot Dam. In section 2.1, it was shown that the initial Ca-chloride composition (i.e. low Na/Cl and SO4/Cl ratios) is gradually modified towards a Mg-chloride water type (higher Na/Cl and SO4/Cl ratios). Given the unique chemical and isotopic compositions that were monitored along the lower Jordan River, it could be suggested that an explanation lies in groundwater discharges into the river. Indeed, water with high Na/Cl and SO4/Cl ratios was found in the saline Yarmouk River, downstream of Adassiya Dam and was suggested to represent the composition of the discharging groundwater. Holtzman et al. (2005) measured the
79 flow rates in this river section and showed a significant contribution of groundwater flux to the lower Jordan River (i.e., a range of 20 to 80% of the river’s measured discharge).
Saline water fraction, f (%) 0204060801005 10 15 0204060801005 10 15 0.95 0.08 Sewage Sewage 0.90 0.07
0.85 0.06 0.80 0.05
0.75 (M/M) /Cl 4 0.04 0.70 Initial SO Na/Cl (M/M) Na/Cl river Initial 0.03 0.65 river Saline 0.60 0.02 Saline
0.55 0.01 0 5000 10000 15000 20000 0 5000 10000 15000 20000
0204060801005 10 15 0204060801005 10 15 3.5 12 Saline Saline 3.0 10
2.5
Initial (M/M) 8 river 4 2.0
6 Initial Ca/SO Ca/Mg (M/M) Ca/Mg 1.5 river
1.0 4 Sewage
Sewage 0.5 2 0 5000 10000 15000 20000 0 5000 10000 15000 20000 Chloride concentration (mg/L)
Fig. 31. Na/Cl, SO4/Cl, Ca/Mg and Ca/SO4 ratios versus chloride concentration of the origin of the river water, as sampled from below Alumot Dam at different times. The measured data are compared to calculated mixing lines between sewage water (as sampled at Bitaniya) and the saline water end member (as sampled at Tiberias Hot Springs). Note that the river composition at Alumot Dam is determined by the mixing relationship between the sewage component (~90%) and the saline component (~10%).
80 Following equation 6, the “f” value was defined as the relative contribution of the Mg-chloride groundwater, Cin as the sulfate content in the initial base flow at Alumot Dam, Cgw as the sulfate content in the saline Yarmouk River (representing the Mg- chloride groundwater in the area), and Cfi as the sulfate content measured at different sites along Segment One of the lower Jordan River. Table 7 presents the f values (%) of the Mg-chloride groundwater and Figure 32A illustrates the variations in this value during the 2 years of water-quality monitoring. The results show an increase in the contribution of the Mg-chloride groundwater, particularly in the spring (Fig. 32A). Since it can be assumed that the groundwater's chemical composition is constant during the year, the variations in the groundwater's salt contribution indicate different rates of groundwater discharge to the river.
Table 7. The contribution of Mg-chloride groundwater (as sampled at the Yarmouk River) to the river flow along the northern section. The calculated results shown here (and in Fig. 32A) were obtained using chloride concentration.
Date Sampling Location Distance from Alumot (km) Yarmouk Fraction (%) 01/09/99 Sheich Hussein Bridge 22.7 48 01/03/00 Hamadiya South 20.1 87 01/05/00 Neve Ur South 12.7 58 01/08/00 Neve Ur North 11.6 44 01/12/00 Hamadiya South 20.1 82 01/02/01 Hamadiya South 20.1 85 01/03/01 Hamadiya North 18.6 51 01/04/01 Hamadiya North 18.6 50 01/06/01 Hamadiya South 20.1 30 01/08/01 Shif'a Station 27.7 9
The variations in groundwater discharge could result from: (1) more irrigation of seasonal crops, which enhances agricultural return flows, and (2) more recharge in the winter months, resulting in increased groundwater discharge. Fig. 32B presents the monthly flow volumes measured from 1990 to 2000 at the Naharaim hydrometric station, adjacent to the confluence of the Yarmouk and lower Jordan rivers (data from Israeli Hydrological Service, 2002). The increased flow rate during the winter months suggests that the overall discharge of surface and groundwater is seasonally controlled (i.e., option #2).
81 100 A 90 80 (%) 70 60 50 40 30
GW Fraction, f f GW Fraction, 20 10 0 Sep-99 Nov-00 Nov-99 Jan-00 Mar-00 May-00 Jul-00 Sep-00 Jan-01 Mar-01 May-01 Jul-01 Mg-chloride
Date
1000 1990/91 B 1991/92 1992/93 1993/94 1994/95 100 1995/96 1996/97 1997/98 1998/99 1999/00 Average Monthly Volume (MCM) Monthly 10
1 Oct Nov Dec Jan Feb Mar Apr May Jun Jul Aug Sep
Fig. 32. (A) Mg-chloride groundwater (GW; as sampled at Yarmouk River) contribution to the lower Jordan River's chemical composition along the northern section of the river, and (B) monthly flow volumes at the Naharaim hydrometric station (in the Yarmouk River), from 1990-2000 (Israeli Hydrological Service, 2002). Note the correspondence between the increases in the discharge of surface and groundwater during the fall and winter months, marked with arrows.
Given that the water quality in the northern segment (Segment One) of the lower Jordan River is controlled by three water components: (1) the saline end member; (2) the sewage end member derived from anthropogenic dumping into the river, and (3) shallow groundwater with a Mg-chloride composition, the relative contributions of these three end members were quantified.
82 2- - Figure 33 plots the calculated composition (SO4 and Cl ) obtained by mixing the three end members and presents the relative contribution (%) of the shallow groundwater to the overall salt balance along Segment One. The three lines connecting the end-member data points (forming a triangle) therefore describe the theoretical mixing lines between the three end members. The data points representing the river's initial base flow (as sampled downstream from Alumot Dam) lie on the line between the saline and sewage end members. Downstream from Alumot Dam, the river data points plot towards the shallow groundwater end member (“Mg-chloride”; Fig. 33). The data show differences in the relative contribution of the shallow groundwater: about 45% in September 1999 (Fig. 33A) and about 80% in December 2000 (Fig. 33B).
83 1000 Sep 1999 THS
800 Mg-chloride 90%
80% 600 80% 70% (mg/L)
4 60% 60% 50% Saline water SO 400 fraction, f (%) 40% 40%
Mg-chloride fraction, f (%) f fraction, Mg-chloride 30% 20% 200 20% River flow Initial river direction 10% Sewage A 0 0 5000 10000 15000 20000 Cl (mg/L) 1000 Dec 2000 THS 800
90%
Mg-chloride 80% 600 70% (mg/L)
4 80% 60%
SO 50% Saline water 400 60% fraction, f (%) 40%
Mg-chloride fraction, f (%) f fraction, Mg-chloride 40% 30% River flow direction 200 20% 20% Initial river 10% Sewage B 0 0 5000 10000 15000 20000 Cl (mg/L)
Fig. 33. Sulfate and chloride concentrations of river samples and an interpretation of the mixing processes occurring among the three end members [i.e., saline spring— as sampled at the Tiberias Hot Springs (THS), sewage—an average of Bitaniya water samples, Mg-chloride groundwater—as sampled at the Yarmouk River, and river water from the initial 20 km as sampled in September 1999 (A) and December 2000 (B)]. Note that as the downstream distance from the lower river's origin increases, the river concentrations move towards the data point representing the shallow groundwater end member ("Mg-chloride"). The groundwater contribution to the water flow of the river varies with time (i.e. in December 2000 the groundwater discharge constituted ~80% of the river flow while in September 1999 it was only ~45%).
84
2.3.3.1.2. Future predictions and management
The current hydrological situation, as described above (i.e. a mixture of three water sources), was used to predict future scenarios. In the following discussion, possible changes in river salinity are evaluated that may be induced by changes in the relative contribution of the different water sources of the lower Jordan River. Several major management scenarios were considered (Table 8): (1) desalination of the SWC and removal of all of the saline sources from the SWC and lower Jordan River; (2) eliminating sewage dumping into the river; (3) differential removal of one of the saline sources from the SWC (i.e. Tabgha Springs or THS); and (4) eliminating both saline sources and sewage dumping into the river. According to Holtzman et al. (2005), the groundwater flux into the river varies from 20 to 80% of the river's flow rate. These values were used as the upper and lower constraints for the groundwater's influence on river salinity. Figure 34A illustrates the mixing combinations between different end members that include sewage, Mg-chloride groundwater, and the two saline water sources: Tabgha Springs (designated “T”) and THS (data from Moise et al., 2000). Line A represents mixing between sewage water and the saline THS. Line B represents mixing between the sewage water and Tabgha Springs, line C represents mixing between THS and the Mg-chloride groundwater as sampled at Yarmouk River, and line D represents mixing between Tabgha Springs and the Mg-chloride groundwater.
85 Table 8. Combinations of lower Jordan River water quality (chloride concentration) and quantity (river discharge) at its origin and 17 km downstream under different management scenarios and with different groundwater (GW) contributions (i.e. 20, 50 and 80%). The right column correlates to the arrows in Figure 34B.
Cl concentration Cl concentration Discharge Arrow No. (meq/L) (mg/L) (MCM/year) in Fig. 8B Tabgha 85 3000 15 Tiberias Hot Springs (THS) 508 18000 1.5 Total Sewage(MNM+Bitaniya) 13 450 13.5 Total Initial River 73 up to 2600 30 Tabgha desalinization 170 6027 1.5 Groundwater Inflow (20%) 32 1150 6 Groundwater Inflow (50%) 32 1150 15 Groundwater Inflow (80%) 32 1150 24 Initial River Present 73 up to 2600 30 1 Removal of all saline water 13 450 13.5 2 Removal of Tabgha 62 2205 15 5 Tabgha desalinization 72 2552 16.5 6 Removal of THS 51 1792 28.5 4 Removal of sewage 123 4364 16.5 3 After 17 km (contribution of 20% GW) Present 67 2360 36 1 Removal of all saline water 19 665 19.5 2 Removal of Tabgha 54 1904 21 5 Tabgha desalinization 61 2178 22.5 6 Removal of THS 47 1680 34.5 4 Removal of sewage 99 3507 22.5 3 After 17 km (contribution of 50% GW) Present 60 2118 45 1 Removal of all saline water 23 818 28.5 2 Removal of Tabgha 47 1678 30 5 Tabgha desalinization 53 1885 31.5 6 Removal of THS 44 1571 43.5 4 Removal of sewage 80 2833 31.5 3 After 17 km (contribution of 80% GW) Present 55 1957 54 1 Removal of all saline water 25 898 37.5 2 Removal of Tabgha 44 1556 39 5 Tabgha desalinization 49 1721 40.5 6 Removal of THS 42 1499 52.5 4 Removal of sewage 69 2459 40.5 3
Figure 34B focuses on the gray zone in Figure 34A and demonstrates the changes in river salinity due to the following scenarios (arrows 2 to 6 in Fig. 34 and Table 8): • All the saline water is removed such that the base flow downstream of Alumot Dam is composed only of low-salinity sewage effluent. Although the downstream river salinity (arrow 2 in Fig. 34B) is expected to increase given
86 the input of the saline groundwater, in this scenario the overall salinity is significantly lower than that of the current situation. • All sewage effluent is removed such that the initial river base flow downstream of Alumot Dam is composed solely of the saline sources. The downstream river salinity will evolve along arrow 3 (Fig. 34B). This is the only scenario in which the river salinity becomes much higher than it is at present. If, however, the sewage effluents are adequately treated and returned to the river, no major change in river salinity will take place. • The THS is selectively removed. The overall salinity of the base flow will be lower than today but the downstream river salinity will evolve to values similar to the current situation (arrow 4 in Fig. 34B). • Tabgha Springs water is selectively removed. The volume of the base flow will significantly decrease but its salinity and the salinity of the downstream river (arrow 5 in Fig. 34B) will be only slightly lower than it is now. • The Tabgha Springs are desalinized at an efficiency of 50%, and the rejected brine (i.e. 50% of the initial volume with twice the original salinity) is diverted into the lower Jordan River. The salinities of the base flow and downstream river are expected to be slightly higher than in the current situation (arrow 6 in Fig. 34B). • All the current inputs that make up the base flow of the lower Jordan River (sewage effluents and saline springs in SWC) are eliminated. The downstream river salinity will therefore be controlled only by the groundwater discharge. The gradual discharge of groundwater into the river will be most pronounced under this scenario, as the flow rate will increase downstream. The composition of the river will not change along the river and will mirror the Mg-chloride of the discharging groundwater. It could be expected that after 12 km, the salinity of the river will be about 1150 mg Cl/L with a maximum flow rate of 24 MCM/year (assuming 80% groundwater discharging). • Overall, it seems that removal of the saline water is the preferred management scenario to obtain the optimal beneficial effects on the river’s ecology, whereas removal of the sewage effluents will have a detrimental effect in terms of river salinity.
87 September 1999
1000
THS Line C 800 Mg-chloride
600 Line D (mg/L) 4 400 SO Line A T B e 200 in L
Sewage A 0 0 5000 10000 15000 20000 Cl (mg/L)
1000
800 Mg-chloride Line C
600 Line D 50%50% contributioncontribution 3 ofof Mg-chlorideMg-chloride 4 5 61 Groundwatergroundwater to to the the 2 400 initialinitial riverriver base flowflow
T 200 Line B Line A
Sewage B 0 0 1000 2000 3000 4000 5000
Cl (mg/L)
Fig. 34. (A) Mixing processes between different end members that include sewage, Mg-chloride groundwater, and two saline water sources, assuming selective removal of one of them. “T” represents the composition of Tabgha Springs. “THS” represents the composition of Tiberias Hot Springs. Line A represents the mixing between sewage water and THS. Line B represents the mixing between sewage water and T. Line C represents the mixing between THS and the Mg-chloride groundwater as sampled at Yarmouk River. Line D represents the mixing between T and the Mg- chloride groundwater. Figure B focuses on the gray zone in Figure A; arrows 1 to 6 represent the variation trends in the river's chemical compositions currently (1) and as a result of the implementation of different scenarios: removal of all the saline water (2); removal of sewage (3); removal of THS (4); removal of T (5), and desalinization of T (6). Note that the slope of the dashed line is derived from Holtzman et al.'s (2005) estimate.
88 2.3.3.2. The southern segment of the lower Jordan River
2.3.3.2.1. Current situation
The southern segment (Segment Two; 66 to 100 km downstream of Alumot Dam; Fig. 28) of the lower Jordan River is characterized by a downstream increase in salinity (Fig. 27). Historical data (Bentor, 1961; Neev and Emery, 1967) indicate that the chloride concentration of the southernmost point of the lower Jordan River at Abdalla Bridge was ~400 mg/L in 1925 and 1947. The present river chloride concentration is in the range of 1500 to 2500 mg/L during most of the year, but can reach up to 5400 mg/L at its southernmost point during the summer months (Farber et al., 2004). Until the 1950s, the estimated Jordan River discharge to the Dead Sea was approximately 1300 MCM/year (Klein, 1995, 1998; Hof, 1998). The current discharge is only 30 to 200 MCM/year (Holtzman et al., 2005; TAHAL, 2000). The significantly reduced flow of the lower Jordan River has resulted in a lowering of the Dead Sea water level by over 20 m in the last 50 years (Gavrieli and Oren, 2004; Hassan and Klein, 2002). To predict the water quality of the southern part of the lower Jordan River under different water-management scenarios, the current hydrological situation must first be determined. The chemical and isotopic compositions of river water in the southern section of the lower Jordan River and the associated inflows and groundwater were investigated in the previous sections. The geochemical data indicated that the river’s quality is largely controlled by non-point discharge of saline groundwater sources. It was demonstrated that the groundwater itself is a mixture of two end members: (1) sulfate-rich saline groundwater; and (2) Ca-chloride Rift Valley brines. The sulfate- rich groundwater is characterized by high Na/Cl (0.81-1.0), SO4/Cl (0.25-0.50), and low Br/Cl (1-4 x 10-3) molar ratios. In contrast, the brines have low Na/Cl (0.55-0.69), -3 SO4/Cl (0.02-0.04), and high Br/Cl (5-9 x 10 ) ratios. Seasonal variations were recognized in the intensity and locations of salinization of the lower Jordan River water. These variations are related to the differential contribution of the two end members' groundwater sources. It was shown that the sulfate-rich groundwater contribution predominates during the spring months in river section A (70-80 km from the river’s origin at Alumot Dam; Fig. 35), while the Ca-chloride brine source affects section B (>75 km; Fig. 35) mostly during the summer months. Chloride
89 concentrations of ~9000 mg/L were estimated for the sulfate-rich groundwater that discharges into the river in section A and 18,700 mg/L for the brines that discharge into section B. The distinction of these two sections enables a quantification of the groundwater discharge by assuming that: (1) groundwater contribution has a distinct discharge, Qgw, and concentration, Cgw, in the two sections, and (2) no sinks or additional sources exist in either of the sections. The chemical variations of the river were used to define two sections during the spring (June) and summer (August) months. Sections A and B are affected by the sulfate-rich groundwater and brines, respectively. In the spring (June), section A lies between the Zarzir site (59.7 km downstream from Alumot Dam; Fig. 35) and the Baptism site (95.6 km; 35.9-km long section), and section B lies between the Baptism site and Abdalla Bridge (100 km; 4.4-km long section). In the summer (August), section A lies between the Zarzir and Gilgal sites (76.6 km; 16.9-km long section) and section B between Gilgal and Abdalla Bridge (23.4-km long section). Following equations 2 and 3, solute mass balances were calculated for the specific sections. For section A, the solute mass balance during the spring (June 2001) is: bp bp = zr zr + gw gw C Q C Q Q1 C1 (8) where Cbp and Czr are chloride concentrations at the end point and initial point of river section A (i.e., Baptism sites and Zarzir; 2720 and 1460 mg/L, respectively).
gw C1 is the sulfate-rich groundwater in section A (8863 mg/L): this value is calculated based on Figure 14 in chapter 2.1 as the intersecting point between lines 1 and 3, which represent the chloride concentration of the groundwater in section A. Qzr is the actual river-discharge measurement carried out in June 2001 (1200 L/s; Holtzman,
gw 2003), and Q1 is the sulfate-rich groundwater discharge in section A. Using this data, the total discharge of river flow was calculated at the end point of section A (i.e., Qbp at Baptism site). This discharge is equal to the total discharges: bp = zr + gw Q Q Q1 (9) For section B, the solute mass balance during the spring (June 2001) is: ab ab = bp bp + gw gw C Q C Q Q2 C2 (10) where Cab and Cbp are the chloride concentrations at the end point and initial point of river section B (i.e., at Abdalla Bridge and Baptism site, 3440 and 2720 mg/L,
gw respectively). C2 is the brine component in section B (18,790 mg/L): this value is
90 calculated based on Figure 14 in chapter 2.1 as the intersecting point between lines 2 and 3, which represent the chloride concentration of the groundwater in section B.
bp gw Q is the value that was calculated previously, Q2 is the Ca-chloride groundwater discharge in section B. Using this data, the total discharge of river flow was calculated at the end point of section B (i.e., Qab at Abdalla Bridge). This discharge is equal to the total discharges: ab = bp + gw Q Q Q2 (11) In the same way, the groundwater discharge was calculated for sections A and B during the summer (August 2001), with section A spanning Zarzir to Gilgal and section B, Gilgal to Abdalla Bridge. For these calculations, the actual river-discharge measurements carried out in August 2001 (300 L/s; Holtzman, 2003) and the chloride concentrations measured in the river concurrently were used. The results indicate that groundwater discharge rates in June 2001 were 246 L/s and 68 L/s for sections A and B, respectively, and in August 2001, they were 39 L/s and 73 L/s, respectively. The data indicate that the groundwater flux (i.e., the discharge divided by the length of every section) is not constant during the year, and that the total flux in June was higher. Following equation 5, the chloride concentration at Abdalla Bridge (i.e., the end point of the river) can be calculated as follows: C zrQ zr + C gwQ gw + C gwQ gw C ab = 1 1 2 2 (12) zr + gw + gw Q Q1 Q2 where the indexes 1 and 2 refer to groundwater in sections A and B, respectively. Thus, the salinity at Abdalla Bridge is directly dependent on the relationships between
zr gw gw the river flow (Q ), the groundwater flow in the two sections (Q1 andQ2 ), and their salinities. Based on equation 12, it can be evaluate how the salinity at Abdalla Bridge would change under different management scenarios.
91 N Lebanon Syria Sea of Upper
Galilee Jordan River Y ar mo uk Israel
Palestinian Authority Jordan Lower Jordan River 55 0 Zarzir E 32 N 0 (W T 35 . ir F t z Dead Sea 60 a a ra Zarqa R. a ) Aug section A 65 25 km
70 Tovlan Adam (Damya) Br. Jun section A Jun section 75 Gilgal 80 Aug section B Aug section W. Mallaha
85 W. Melecha
Uga 90
W. Nueima Allenby Br. 95 June B W. Kelt 100 Baptism site Legend km Abdalla Br. River sampling site Dead Sea Bridge crossing
Fig. 35. Detailed map of the southern part of the lower Jordan River, including river segments for June and August 2001.
92 2.3.3.2.2. Future predictions and management
The different management scenarios considered for Segment One of the lower Jordan River (from Alumot Dam to Adam Bridge) was also applied to Segment Two. The final point of Segment One (66 km downstream of Alumot Dam) was used as a starting point for Segment Two. The chloride concentration, Cab, at Abdalla Bridge was calculated for two different conditions: “August” and “June”. The previously calculated groundwater discharges were used (i.e., 246 L/s in section A and 68 L/s in section B for the “June condition”; 39 L/s in section A and 73 L/s in section B for the “August condition”). The groundwater chloride concentrations for the sulfate-rich groundwater and for the Ca-chloride groundwater were 8863 and 18,790 mg/L, respectively. Czr for the starting point of Segment Two is the same as the chloride concentration of the end point of Segment One, and varies according to the different management scenarios outlined for the latter segment. Table 9 summarizes the effects of the different scenarios on the salinity and river discharge at Abdalla Bridge. The results of all but one (removal of THS) of the management scenarios indicate a significant reduction in the discharge flow of the river relative to the present situation (Table 8). Thus, the current ratio between the surface-water and groundwater discharge is expected to decrease and the saline groundwater contribution to increase. Consequently, the salinity differences between the upstream river (before groundwater discharge) and downstream river will also increase and the effect of the saline groundwater discharge will be more pronounced, leading to the further salinization of the downstream part of the lower Jordan River. The current flow of the Jordan River to the Dead Sea is approximately 30-200 MCM/year (Holtzman et al, 2005; TAHAL, 2000). According to Table 8, most of the future management scenarios will cause a reduction of 14-16 MCM/year. Thus, it is predicted that implementation of these management scenarios will cause a further decrease in river flow to the Dead Sea. Table 9 summarizes the chloride concentrations of the river under different management scenarios, based on the discharge values measured in June and August 2001. During these 2 months, the chloride concentration at Abdalla Bridge was 3440 and 5370 mg/L, respectively. According to our “June calculations”, removal of all of the saline water from the lower Jordan River would reduce the chloride concentration to 3000 mg/L, whereas removal of the sewage from the lower river's origin would increase the chloride concentration to ~5000 mg/L at Abdalla Bridge. According to
93 our “August calculations”, removal of all the saline water from the lower river's origin would reduce the chloride concentration to 5200 mg/L, whereas removal of the sewage would increase the chloride concentration to ~7000 mg/L at Abdalla Bridge. Therefore, the ability to utilize the river water in the future depends on the river's management at the initial point of the lower Jordan River, at Alumot Dam. Removal of the upstream saline water would have the most beneficial effect on the river's ecological system, whereas removal of the sewage water would have detrimental effects in terms of river salinity.
94 Table 9. Combinations of lower Jordan River water quality (chloride concentration) and quantity (river discharge) under different management scenarios and groundwater (GW) contributions. Calculated values are based on June and August 2001 discharge measurements, and the different scenarios refer to the present situation and removal one of the river's initial end-member sources. Qi—river discharge at the initial sample site (Zarzir Station), Ci—river chloride concentration at the initial sample site (Zarzir Station), Q1—GW discharge at Segment One, C1— GW chloride concentration at Segment One, Q2—GW discharge at Segment Two, C2—GW chloride concentration at Segment Two, Q3—river discharge at the final sample site (Abdalla Bridge), C3—river chloride concentration at the final sample site (Abdalla Bridge).
Qi Ci Q1 C1 Q2 C2 Q3 C3 L/s mg/L L/s mg/L L/s mg/L L/s mg/L Jun-01 1200 1461 246 8863 68 18790 1514 3439 After 17 km (contribution of 20% GW) Removal of all saline water 1080 674 246 8863 68 18790 1394 2999 Removal of Tabgha 1080 1914 246 8863 68 18790 1394 3961 Tabgha desalinization 1080 2163 246 8863 68 18790 1394 4153 Removal of Tiberias Hot Springs (THS) 1200 1666 246 8863 68 18790 1514 3602 Removal of sewage 1080 3510 246 8863 68 18790 1394 5197 After 17 km (contribution of 50% GW) Removal of all saline water 1080 815 246 8863 68 18790 1394 3109 Removal of Tabgha 1080 1666 246 8863 68 18790 1394 3769 Tabgha desalinization 1080 1879 246 8863 68 18790 1394 3933 Removal of THS 1200 1560 246 8863 68 18790 1514 3518 Removal of sewage 1080 2836 246 8863 68 18790 1394 4675 After 17 km (contribution of 80% GW) Removal of all saline water 1080 886 246 8863 68 18790 1394 3164 Removal of Tabgha 1080 1560 246 8863 68 18790 1394 3686 Tabgha desalinization 1080 1737 246 8863 68 18790 1394 3823 Removal of THS 1200 1489 246 8863 68 18790 1514 3461 Removal of sewage 1080 2446 246 8863 68 18790 1394 4373
95 Qi Ci Q1 C1 Q2 C2 Q3 C3 L/s mg/L L/s mg/L L/s mg/L L/s mg/L Aug-01 300 1659 39 8863 73 18790 412 5371 After 17 km (contribution of 20% GW) Removal all the Saline water 270 674 39 8863 73 18790 382 4966 Removal Tabgha 270 1914 39 8863 73 18790 382 5844 Tabgha desalinization 270 2163 39 8863 73 18790 382 6019 Removal Tiberias Hot Springs 300 1666 39 8863 73 18790 412 5376 Removal Sewage 270 3510 39 8863 73 18790 382 6972 After 17 km (contribution of 50% GW) Removal of all saline water 270 815 39 8863 73 18790 382 5066 Removal of Tabgha 270 1666 39 8863 73 18790 382 5668 Tabgha desalinization 270 1879 39 8863 73 18790 382 5818 Removal of THS 300 1560 39 8863 73 18790 412 5299 Removal of sewage 270 2836 39 8863 73 18790 382 6496 After 17 km (contribution of 80% GW) Removal of all saline water 270 886 39 8863 73 18790 382 5116 Removal of Tabgha 270 1560 39 8863 73 18790 382 5593 Tabgha desalinization 270 1737 39 8863 73 18790 382 5718 Removal of THS 300 1489 39 8863 73 18790 412 5247 Removal of sewage 270 2446 39 8863 73 18790 382 6220
2.3.4. Conclusions This section aims to predict future salinity variations of the lower Jordan River under several different management scenarios that are included in the peace treaty between Israel and Jordan. The predictions are based on understanding the relationships between shallow groundwater and surface-water flow in the Jordan River. For the calculations of the future scenarios, differential removal of the water sources (sewage and saline waters) that make up the initial flow of the Jordan River was considered. Removal of sewage effluents and saline water are the principal elements mentioned in the peace treaty between Israel and Jordan with respect to future joint-management activities. Whereas the data on actual discharge flow in the Jordan River is limited (Holtzman et al., 2005), recently published geochemical data was used to quantify the relationships between groundwater flux and river flow.
96 The salinity of the initial river (at Alumot Dam) is currently up to 2600 mg Cl/L, and depends primarily on the relationships between natural saline water and sewage effluents that are dumped into the river. The calculations show that removal of the sewage effluent from the lower Jordan River will increase its salinity (to ~4400 mg Cl/L), whereas removal of the saline component will reduce it (to ~450 mg Cl/L) at Alumot Dam. Current shallow groundwater discharge to the northern section (Segment One) of the lower Jordan River buffers river quality and reduces river salinity. The river salinity decreases downstream from 2360 to 2000 mg Cl/L (with 20%-80% groundwater contribution, respectively) about 20 km downstream of Alumot Dam. Removal of the sewage component will cause a downstream increase in river salinity (to ~3500 mg Cl/L), whereas removal of the saline component will cause a downstream reduction in salinity (to ~665 mg Cl/L). These predictions indicate that the northern part (Segment One) of the lower Jordan River could turn into a low- saline river if the current saline component is removed. In this case, the river will be suitable for almost all types of agricultural applications (but will have limited water for this purpose due to a decrease in river flux). In contrast, the salinity of the lower Jordan River could increase upon removal of the sewage effluents and thus its suitability for different agricultural crops would be further limited. The different management scenarios that are applied to the northern area of the lower Jordan River are also valid for the southern part (Segment Two; 66-100 km downstream from Alumot Dam). For this part of the river, the estimation was based on two discharge measurements that were carried out in June and August 2001 at Zarzir Station (66 km downstream from Alumot Dam; Holtzman et al., 2005) and solute mass balance assuming that groundwater discharge is the major source of salinization of the river in this section. The current salinity of the southernmost point of the lower Jordan River at Abdalla Bridge is 3440 and 5370 mg Cl/L (June and August 2001, respectively). These calculations indicate that removal of the saline component at the initial point of the river at Alumot Dam would cause only a small change in the downstream river's salinity (decrease from 3440 to 3000 mg Cl/L in June and 5370 to 5000 mg Cl/L in August), given the large contribution of the saline groundwater. However, selective removal of the sewage component would cause a significant increase in the downstream river's salinity. Under this scenario, the river salinity at Abdalla Bridge would increase to 5200 mg Cl/L in June, 7000 mg Cl/L in August.
97 Overall, the predictions indicate that the future of the lower Jordan River depends directly on the different management activities suggested by the peace treaty between Israel and Jordan. Two opposite trends are shown upon elimination of the saline water or sewage effluents from the river. The continuation and possible increase in sewage drainage into the river, combined with elimination of saline water discharge, will significantly reduce river-water salinity and will increase its suitability for different agricultural uses. In contrast, selective removal of the sewage component will reduce the surface flow, increase the contribution of the saline groundwater in the southern part of the river, and consequently, increase the river's salinity. It can be concluded that the sewage inflow into the lower Jordan River is a vital component in maintaining and even reducing the river's salinity. Nonetheless, discharge of sewage effluents could contribute organic contaminants. Therefore, one might recommend improving the treatment of sewage effluents being discharged into the river in order to improve other elements of river quality.
98 3. Summary
Although river salinization phenomena have been reported for major river basins around the world, such as the Colorado River (Pillsbury, 1981), Arkansas River (Gates et al., 2002), Nile River (Kotb et al., 2000), the Euphrates and Tigris rivers (Fattah and Abdul Baki, 1980; Robson et al., 1983), and the Murray River (Allison et al., 1990; Herczeg et al., 1993), only a few studies (Herczeg et al., 1993; Phillips et al., 2003) have used geochemical and isotopic tools to define the sources of the solutes affecting the river's quality. Indeed, different sources of salts have been postulated for river salinization. In the Murray-Darling Basin in South Australia, soluble aerosols derived from the ocean are deposited in the drainage basin, concentrated by evapotranspiration and discharged into the Murray River (Allison et al., 1990; Herczeg et al., 1993). In contrast, the riverine salts can also be derived from leaching of evaporitic rocks as demonstrated in the southern Rio Grande Basin in the US (Phillips et al., 2003). In the lower Jordan River, between the Sea of Galilee and the Dead Sea, integration of several geochemical and isotopic tracers was an essential tool in distinguishing the multiple sources that can affect the salt content of river systems. Along the research a wide range of stable isotopes were used, together with major ions and trace elements in order to (1) identify and characterize the water source, and (2) quantify the contribution of different adjacent water sources to the river's discharge. The identification of the different sources was based on the combination between the isotopic and chemical data. The quantification, however, was based mainly on the chemical data rather than the isotopic. Upstream diversion of the natural river sources (Sea of Galilee, Yarmouk River, and Zarqa River) has resulted in a significant reduction in the surface discharge of the river (30 to 200 MCM/year relative to >1300 MCM/year a century ago). In addition, low-quality water sources (saline water, sewage effluents) are being artificially dumped into the river. 87 86 11 34 18 Based on chemical and isotopic ( Sr/ Sr, δ B, δ Ssulfate, δ Owater) compositions of water from the lower Jordan River and its major tributaries, three separate hydrological zones were identified along the river's flow: • A northern section (20 km downstream from its source) where the initial saline base flow, composed of artificial recharge of saline and waste waters, is
99 modified due to discharge of shallow sulfate-rich groundwater, characterized 87 86 34 11 by low Sr/ Sr (0.7072), δ Ssulfate (-2‰), high δ B (~36‰) and high 18 δ Owater (-2 to –3‰) values. The shallow groundwater is derived from agricultural drainage water mixed with natural saline groundwater and discharges into both the Jordan and Yarmouk rivers. The contribution of the groundwater component to the Jordan River flow, deduced from mixing relationships of solutes and strontium isotopes, varies from 20 to 50% of the total. • A central zone (20-60 km downstream from its source), where salinity 87 86 variations are minimal and the rise of Sr/ Sr and SO4/Cl ratios reflect predominance of eastern surface flows. • A southern section (60-100 km downstream of its source), where the salinity of the lower Jordan River increases, particularly during the spring (70-80 km) and summer (80-100 km) to TDS values as high as 11.1 g/L. Variations in the chemical and isotopic compositions of river water along the southern section suggest that the Zarqa River (87Sr/86Sr ~ 0.70865; δ11B ~ 25‰) has a negligible affect on the salinity of the lower Jordan River. Instead, the river quality is influenced primarily by groundwater discharge composed of sulfate- - - rich saline groundwater (Cl = 31-180 mM; SO4/Cl ~ 0.2-0.5; Br/Cl ~ 2-3 x 10 3 87 86 11 34 ; Sr/ Sr ~ 0.70805; δ B ~ 30‰; δ Ssulfate = 4-10‰), and Ca-chloride Rift Valley brines (Cl- = 846-1500 mM; Br/Cl ~ 6-8 x 10-3; 87Sr/86Sr ~ 0.7080; 11 34 δ B > 40‰; δ Ssulfate = 4-10‰). Mixing calculations indicate that the groundwater discharging into the river is composed of different proportions of brines and sulfate-rich saline groundwater. Solute mass-balance calculations indicate a ~10% contribution of saline groundwater (Cl- = 282 to 564 mM) to the river's salt discharge. These findings suggest that shallow groundwater and hypersaline brines are the two dominant factors controlling the chemical composition of the lower Jordan River. In light of this finding, the geochemistry of groundwater resources in the Jordan Valley and the impact of the Rift Valley brines were investigated in detail. Until now, only limited data had been reported on the brine's existence between the Sea of Galilee and the Dead Sea, and its role in this area on river salinization had not been studied. Therefore, the chemical composition of shallow groundwater was characterized. This characterization assisted in an evaluation of the overall impact of
100 the deep hypersaline brines on the geochemistry of shallow groundwater in the Jordan Valley. This study maps the different water bodies along the river and shows that the deep hypersaline brines flow into shallow groundwater systems and significantly affect these systems' quality and chemical composition. Geographical-chemical trends in ions ratios were observed in the brines. These trends were consistent with a larger- scale south-to-north shift in the ionic ratios of the Rift Valley brines reported in previous studies. In addition to the brine, the low-salinity groundwater was studied. This groundwater was divided into three different groups, each having its unique chemical and isotopic characteristics as well as different geographic locations. The three different water groups were: • Group A—a Na-chloride freshwater group characterized by a low 87Sr/86Sr ratio (0.70693-0.70758). This water group was detected in the northern section of the research area. • Group B—a saline to hypersaline water group, characterized by an intermediate 87Sr/86Sr ratio (0.70778-0.70820). This group was divided into three subgroups, based on their chemical compositions (i.e., ion ratios and sulfur isotopes) and their geographic distribution in the Jordan Valley: Subgroup B1—a Na-chloride water type characterized by low salinity. This subgroup was detected in the northern section of the research area. Subgroup B2—a Na-chloride water type. This subgroup was detected mainly in the central section of the research area (50-60 km downstream of Alumot Dam). Subgroup B3—a Mg-chloride water type. This subgroup was detected in the southern section of the research area (66-100 km downstream of Alumot Dam). • Group C—a Mg-chloride saline water, characterized by a high 87Sr/86Sr ratio (0.70857-0.70871). This water group was detected in the southern section of the research area.
An evaluation of the salinity sources of the lower Jordan River and groundwater resources in the Jordan Valley has direct implications for future management of the
101 Jordan River. This concern was addressed in 1994 by the peace treaty between Israel and Jordan. In the treaty, the two countries agreed to increase and equalize the overall pumping rights, to eliminate wastewater disposal into the river, and to use the saline water that currently flows into the river for desalination. The geochemical and hydrological findings show that the water quality of the base flow of the lower Jordan River is dependent upon the ratio between surface-water flow and groundwater discharge. Using water-quality data, mass-balance calculations, and actual flow-rate measurements, possible management scenarios for the lower Jordan River and their potential effects on its salinity were investigated. The theoretical scenarios reveal that implementation of some elements of the Israel-Jordan Peace Treaty would have negative effects on the Jordan River's water salinity. The predictions show that removal of sewage effluents dumped into the river (~13 MCM/year) will significantly reduce the river water’s flow and increase the relative proportion of the saline groundwater flux into the river. Under this scenario, the chloride content of the river at its southern point (Abdalla Bridge) will rise to almost 7000 mg/L during the summer. In contrast, removal of all the saline water (16.5 MCM/year) that is artificially discharged into the lower Jordan River would significantly reduce its chloride concentration, to levels of 650 to 2600 mg/L and 3000 to 3500 mg/L in the northern and southern areas of the lower Jordan River, respectively. However, because removal of either the sewage effluents or the saline water will decrease the river’s discharge to a level that could potentially cause river desiccation during the summer months, other water sources must be allocated to preserve in-stream flow needs and hence the river’s ecosystem.
102 4. References
Allison, G.B., Cook, P.G., Barnett, S.R., Walker, G.R., Jolly, I.D. and Hughes, M.W., 1990. Land clearance and river salinization in the western Murray basin, Australia. J. Hydrol. 119, pp. 1–20.
Austin, S. A., 1992. Isotope and trace element analysis of hypersthene-normative basalts from the Quaternary of Uinkaret Plateau, western Grand Canyon, Arizona. Geological Society of America Abstracts with Programs 24, 261.
Beaumont, P., 1996. Agricultural and environmental changes in the upper Euphrates catchment of Turkey and Syria and their political and economic implications. Applied Geography 16, pp. 137–157.
Begin, Z. B., 1975. The Geology of Jericho Sheet. Isr. Geol. Surv. Bulletin 67.
Begin, Z. B., Ehrlich, A. and Nathan, Y., 1974. Lake Lisan: the Pleistocene precursor of the Dead Sea. Isr. Geol. Surv. Bulletin 63.
Bender, F., 1968. Geologie von Jordanien. Gebrüder Borntraeger, Berlin.
Bender, F., 1974. Geology of Jordan, English Edition. Gebrüder Borntraeger, Berlin.
Bentor, Y. K., 1961. Some geochemical aspects of the Dead Sea and the question of its age. Geochim. Cosmochim. Acta 25, 239-260.
Bentor, Y. K. and Vroman, A., 1960. The geological map of Israel, on a 1:100,000 scale. Series A- The Negev. Sheet 16: Mt. Sdom. Geol. Isr.
Bullen, T. D., Krabbenhoft, D. P. and Kendall, C., 1996. Kinetic and mineralogic controls on the evolution of groundwater chemistry and 87Sr/86Sr in a sandy silicate aquifer, northern Wisconsin, USA. Geochim. Cosmochim. Acta 60, 1807-1821.
Coleman, M.L. and Moore, M.P., 1978. Direct reduction of sulfate to sulfur dioxide for isotopic analysis. Anal. Chem. 50, pp. 1594–1595.
Craig, H., 1961. Standard for reporting concentrations of deuterium and oxygen-18 in natural waters. Science 133, pp. 1833–1834.
Cullen, H.M., deMenocal, P.B., Hemming, S., Hemming, G., Brown, F.H., Guildeson, T., and Sirocko, F., 2000. Climate change and the collapse of the Akkadian empire: evidence from deep sea. J. Geol. 28, pp. 379–382. deMenocal, P.B., 2001. Cultural responses to climate change during the Late Holocene. J. Sci. 292, pp. 667–669.
EXACT, 1998. Overview of Middle East Water Resources: Water resources of Palestinian, Jordanian and Israeli interest. Jordanian Ministry of Water and Irrigation, Palestinian Water Authority and Israeli Hydrological Service. A Report Compiled by
103 the U.S. Geological Survey for the Executive Action Team, Middle East Water Data Banks Project [http://exact-me.org/overview/index.htm].
Farber, E., Vengosh, A., Gavrieli, I., Marie, A., Bullen, T.D., Mayer, B., Holtzman, R., Segal, M., and Shavit, U., 2004. Hydrochemistry and isotope geochemistry of the lower Jordan River: constraints for the origin and mechanisms of salinization. Geochim. Cosmochim. Acta 68, pp.1989–2006.
Farber, E., Vengosh, A., Gavrieli, I., Marie, A., Bullen, T.D., Mayer, B., Holtzman, R., Segal, M., and Shavit, U., 2005. Management scenarios for the Jordan River salinity crisis. Appl. Geochem. 20, pp. 2138–2153.
Farber, E., Vengosh, A., Gavrieli, I., Marie, A., Bullen, T.D., Mayer, B., Polak, A. and Shavit, U. The geochemistry of groundwater resources in the Jordan Valley: The impact of the Rift Valley brines. Accepted to Applied Geochemistry.
Fattah, Q.N. and Abdul Baki, S.J., 1980. Effects of drainage systems on water quality of major Iraqi rivers. Internat. Assoc. Hydrol. Sci. Publ. 130, pp. 265–270.
Freund, R., Garfunkel, Z., Zak, I., Goldberg, M., Weissbrod, T. and Derin, B., 1970. The shear along the Dead Sea rift. Philos. Trans. R. Soc. Lond. A 267, 107-130.
Fritz, B., Clauer, N. and Kam, M., 1987. Strontium isotopic data and geochemical calculations as indicators of the origin of saline waters in crystalline rocks. In: P. Fritz and S. R. Frape (Editors) Saline Water and Gases in Crystalline Rocks, Special Paper 33, Geol. Assoc. of Canada, 121-126.
Garfunkel, Z., 1981. Internal structure of the Dead Sea leaky transform (rift) in relation to plate kinematics. Tectonophysics 80, 81-108.
Garfunkel, Z. and Ben-Avraham, Z. 1996. The structure of the Dead Sea basin. Tectonophysics 266, 155-176.
Gates, T.K., Burkhalter, J.P., Labadie, J.W., Valliant, J.C., and Broner, I., 2002. Monitoring and modelling flow and salt transport in a salinity-threatened irrigated valley. Journal of Irrigation and Drainage Engineering, ASCE, 128, pp. 87–99.
Gavrieli, I., Stein, M., Kolodny, Y. and Spiro, B., 1998. Sulfur isotopes in gypsum as indicator for paleolimnological conditions of Lake Lisan, the Dead Sea Rift Valley, Am. Geophys. Union. Fall Meet., San Francisco, CA, F521.
Gavrieli, I., Yechieli, I., Halicz, L., Spiro, B., Bein, A. and Efron. D., 2001. The sulfur system in anoxic subsurface brines and its implication in brine evolutionary pathways: the Ca-chloride brines in the Dead Sea area. Earth and Planetary Science Letters 186, 199-213.
Gavrieli, I. and Oren, A., 2004. The Dead Sea as a dying lake. In: J.C.J. Nihoul, P.O. Zavialov, and P.P. Micklin (Editors) Dying and Dead Seas. Climatic Versus Anthropic Causes. Kluwer Academic Publishers, Dordrecht, pp. 287–305.
104 Gavrieli, I. and Stein, M., in prep. The origin and fate of the brines in the Dead Sea basin. In GSA Special Paper on the Dead Sea (Eds. Enzel Y., Agnon A. and Stein M.). In preparation.
Goldschmidt, M. J., Arad, A. and Neev, D., 1967. The mechanism of the saline springs in the Lake Tiberias depression. Geol. Surv. Isr. Bulletin 45.
Gropius, M. and Klingbeil, R., 1999. Hydrogeological and Geophysical Investigation in Jericho Area. DGG-Meeting on Environmental Geophysics, Neustadt, Germany.
Hassan, M. and Klein, M., 2002. Fluvial adjustment of the Lower Jordan River to a drop in the Dead Sea level. Geomorphology 45, pp. 21–33.
Hazan, N., 2003. Reconstruction of Kinneret Lake. Levels in the last 40,000 years. M.Sc. Thesis, The Hebrew University of Jerusalem, Israel.
Herczeg, A.L., Simpson, H.J., and Mazor, E., 1993. Transport of soluble salts in a large semi-arid basin: River Murray, Australia. J. Hydrol. 144, pp. 59–84.
Hof, F.C., 1998. Dividing the Yarmouk’s waters: Jordan’s treaties with Syria and Israel. Water Policy 1, pp. 81–94.
Holtzman, R., 2003. Water quality and quantities along the Jordan River—salinization sources and mechanisms. (In Hebrew; tables, figures, and references in English.) M.Sc. Thesis, Technion, Haifa, Israel.
Holtzman, R., Shavit, U., Segal-Rozenhaimer, M., Gavrieli, I., Farber, E., and Vengosh, A., 2005. Quantifying Ground Water Inputs along the Lower Jordan River. J. Environ. Qual. 34(3), pp. 897-906.
Israeli Hydrological Service, 2002. Report of Discharge Measurements from Naharayim Hydrometer Station (No. 34185). Water Commissionership, Ministry of National Infrastructure, Tel Aviv.
Israel-Jordan Peace Treaty, Annex II, 1994. Water Related Matters (http://www.us- israel.org/jsource/Peace/annex2.html) (verified 4 April 2004). Governments of Israel and Jordan.
Katz, A., Kolodny, Y. and Nissenbaum, A., 1977. The geochemical evolution of the Pleistocene Lake Lisan-Dead Sea system. Geochim. Cosmochim. Acta 41, 1609- 1626.
Katz, A. and Kolodny, N. 1989. Hypersaline brine diagenesis and evolution in the Dead Sea-Lake Lisan system (Israel). Geochim. Cosmochim. Acta, 53, 59-67.
Klein, M., 1995. The adjustment of the meandering pattern of the Lower Jordan River to change in water discharge. Earth Surface Processes Landforms 10, pp. 525–531.
Klein, M., 1998. Water balance of the Upper Jordan River basin. Water International 23, pp. 244–248.
105 Klein-BenDavid, O., Sass, E. and Katz. A., 2004. The evolution of marine evaporitic brines in inland basins: the Jordan-Dead Sea Rift valley. Geochim. Cosmochim. Acta 68, 1763-1775.
Kolodny, Y., Katz, A., Starinsky, A., Moise, T. and Simon, E., 1999. Chemical tracing of salinity sources in Lake Kinneret, Israel. Limnol. Oceanogr. 44, 1035-1044.
Kotb, T.H.S., Watanabe, T., Ogino, Y., and Tanji, K.T., 2000. Soil salinization in the Nile Delta and related policy issues in Egypt. Agric. Water Manag. 43, pp. 239–261.
Krasheninnikov, V.; Hall, J.K.; Hirsch, F.; Benjamini, C. and Flexer, A. (eds.), 2005. Geological Framework of the Levant, Volume II: The Levantine Basin and Israel. Historical Productions-Hall, Jerusalem. ISBN 965-7297-02-8.
Krumgalz, B. S., Hecht, A., Starinsky, A. and Katz, A., 2000. Thermodynamic constraints on Dead Sea evaporation: Can the Dead Sea dry up? Chem. Geol. 165, 1- 11.
Landmann, G., Abu Qudaira, G.M., Shawabkeh, K., Wrede, V. and Kempe, S., 2002. Geochemistry of the Lisan and Damya Formation in Jordan, and implications for paleoclimate. Quaternary Inter. 89, 45-57.
Levitte, D., Olshina, A. and Wachks, D., 1978. Geological and geophysical investigation in the Hammat Gadder hot springs area. Isr. Geol. Surv., Rep. Hydro. 4/78.
Linnerooth, J., 1990. The Danube River Basin: negotiation settlements to transboundary environmental issues. Nature Res. J. 30, pp. 629–660.
Marie, A. and Vengosh, A., 2001. Sources of salinity in groundwater from Jericho area, Jordan valley. J. Ground Water 39, pp. 240–248.
McCaffrey, M. A., Lazar, B. and Holland, H. D., 1987. The evaporation path of seawater and the coprecipitation of Br- and K+ with halite. Jour. Sediment. Petrol. 57/5, 928-937.
Moise, T., Starinsky, A., Katz, A. and Kolodny, Y., 2000. Ra isotopes and Rn in brines and ground waters of the Jordan-Dead Sea Rift Valley: enrichment, retardation, and mixing. Geochim. Cosmochim. Acta 64, 2371-2388.
Möller, P., Rosenthal, E., Dulski, P., Geyer, S., and Guttman, Y., 2003. Rare earths and yttrium hydrostratigraphy along the Lake Kinneret-Dead Sea-Arava transform fault, Israel and adjoining territories. Appl. Geochem. 18, pp. 1613–1628.
Mook, W. G., 2000. Introduction; theory, methods, review. Volume I in Mook, W. G. (ed.), Environmental Isotopes in the Hydrological Cycle. UNESCO/IAEA, Paris/ Vienna.
Neev, D. and Emery, K. O., 1967. The Dead Sea; depositional processes and environments of evaporites. Isr. Geol. Surv. Bulletin 41, 1-147.
106 Nishri, A., Stiller, M., Rimmer, A., Geifman Y. and Krom, M., 1999. Lake Kinneret (The Sea of Galilee): the effects of diversion of external salinity sources and the probable chemical composition of the internal salinity sources. Chem. Geol. 158, 37- 52.
Nissenbaum, A., 1969. Studies in the Geochemistry of the Jordan River Dead Sea System. Ph.D. Dissertation, University of California, Los Angeles.
Parker, D. H., 1970. The hydrogeology of the Mesozoic and Cenozoic aquifers of the western highlands and plateau of East Jordan (4 vols). United Nations Development Program/Food and Agriculture Organization, Technical Report 212, 1-424.
Parkhurst, D. L. and Appelo, C. A. J., 1999. User's guide to PHREEQC (Version 2) - a computer program for speciation, batch-reaction, one-dimensional transport, and inverse geochemical calculations. U.S. Geol. Surv Water-Resources Investigations Report 99-4259.
Phillips, F.M., Hogan, J.F., Mills, S.K., and Hendrickx, J.M.H., 2003. Environmental tracers applied to quantifying causes of salinity in arid-region rivers: preliminary results from the Rio Grande, Southwestern USA. In: Water Resources Perspectives: Evaluation, Management and Policy, edited by A.S. Alsharhan and W.W. Wood, New York, Elsevier Science, pp. 327-334.
Picard, L., 1943. Structure and evolution of Palestine; with comparative notes on neighbouring countries. Hebrew Univ., Jerusalem, Geol. Dept., Vol. 4, no. 2-4.
Picard, L., 1965. The geological evolution of the Quaternary in the central-northern Jordan graben, Israel, in Wright, H. E. and Frey, D. G., International studies on the quaternary; papers prepared on the occasion of the VII Congress of the International Association for Quaternary Research, Boulder, Colorado, 1965. Geol. Soc. Am., Spec. Pap. 84, 337-366.
Pillsbury, A.F., 1981. The salinity of rivers. Sci. Am. 245, pp. 54–65.
Pufahl, P. K., Grimm, K. A., Abed, A. M., and Sadaqah, R. M. Y., 2003. Upper Cretaceous (Campanian) phosphorites in Jordan: implications for the formation of a south Tethyan phosphorite giant. Sedimentary Geol. 161, 175-205.
Raab, M., Friedman, G. M., Spiro, B., Starinsky, A. and Zak, I., 1997. The geological history of Messinian (upper Miocene) evaporites in the central Jordan Valley (Israel) and how strontium and sulfur isotopes relate to their origin. Carbonates and Evaporites 12, 296-324.
Robson, J.F., Stoner, R.F., and Perry, J.H., 1983. Disposal of drainage water from irrigated alluvial plains. Water Sci. Tech. 16, pp. 41–55.
Rosenthal, E., 1987. Chemical composition of rainfall and groundwater in recharge areas of the Bet Shean-Harod multiple aquifer system, Israel. J. Hydrol. 89, 329–352.
Salameh, E., 1996. Water quality degradation in Jordan. Friedrich Ebert Stiftuns and Royal Society for Conservation of Nature, Amman, Jordan, p. 179.
107
Salameh, E., 2002. Sources of water salinities in the Jordan Valley Area/ Jordan. Acta Hydrochim. Hydrobiol. 29, 329-362.
Salameh, E., and Naser, H., 1999. Does the actual drop in Dead Sea level reflect the development of water resources within its drainage basin? Hydrochim. Hydrobiol. Acta 27, pp. 5-11.
Schmandt, J., 2002. Bi-national water issues in the Rio Grande/Rio Bravo basin. Water Policy 4, pp.137–155.
Segal-Rozenhaimer, M., Shavit, U., Vengosh, A., Gavrieli, I., Farber, E., Holtzman, R., Mayer, B., and Shaviv, A., 2004. Sources and Transformations of Nitrogen Compounds along the Lower Jordan River. Journal of Environmental Quality, 33, 1440-1451.
Shavit, U., Holtzman, R., Segal, M., Vengosh, A., Farber, E., Gavrieli, I., ECO- Research Team, and Bullen, T., 2002. Water sources and quality along the Lower Jordan River, regional study. In: H. Rubin et al. (Editors) Water Resources Quality, Preserving the Quality of Our Water Resources. Springer-Verlag, Berlin. pp. 127– 148.
Shmueli, D.F., 1999. Water quality in international river basins. Political Geography 18, pp. 437–476.
Silva, S.R., Kendall, C., Wilkison, D.H., Ziegler, A.C., Chang, C.C.Y., and Avanzino, R.J., 2000. A new method for collection of nitrate from fresh water and analysis of the nitrogen and oxygen isotope ratios. J. Hydrol. 228, pp. 22–36.
Simon, E. and Mero, F., 1992. The salinization mechanism of Lake Kinneret. J. Hydro. 138, 327-343.
Stanislavsky, E. and Gvirtzman, H., 1999. Basin-scale migration of continental-rift brines: paleohydrologic modeling of the Dead Sea basin. Geology 27, 791-794.
Starinsky, A., 1974. Relationship between Ca-chloride brines and sedimentary rocks in Israel. Ph.D. Thesis, The Hebrew University of Jerusalem (in Hebrew, Engl. abstract).
Stein, M., Garfunkel, Z. and Jagoutz, E., 1993. Chronothermometry of peridotitic and pyroxenitic xenoliths: Implications for the thermal evolution of the Arabian lithosphere. Geochim. Cosmochim. Acta 57, 1325-1337.
Stein, M., Starinsky, A., Katz, A., Goldstein, S. L., Machlus, M. and Schramm, A., 1997. Strontium isotopic, chemical, and sedimentological evidence for evolution on Lake Lisan and the Dead Sea. Geochim. Cosmochim. Acta 61, 3975-3992.
Stein, M., Starinsky, A., Agnon, A., Katz, A., Raab, M., Spiro, B. and Zak, I., 2000. The impact of brine-rock interaction during marine evaporite formation on the isotopic Sr record in the oceans: evidence from Mt. Sedom, Israel. Geochim. Cosmochim. Acta 64, 2039-2053.
108
Stein, M., Agnon, A., Ben Avraham, Z., Goldstein, S., and Negendank, J. 2005. The Dead Sea as a Global Paleo-Environmental Archive: The Prospects of Scientific Deep Drill. ICDP Conference of Continental Scientific Drilling 2005: A Decade of Progress and Opportunities for the Future. Potsdam, February 2005.
TAHAL, Israeli Water Division Office, Israeli Office of National Foundation, TAHAL-Consulting Engineering LTD., 2000. Flows in the Lower Jordan River. Report for the Office of National Foundation, 6130-d00.385.
Torfstein, A., Gavrieli, I. and Stein, M., 2005. The sources and evolution of sulfur in the hypersaline Lake Lisan (paleo-Dead Sea). Earth and Planetary Sci. Lett. 236, 61- 77.
Vengosh, A., Kolodny, Y., Starinsky, A., Chivas, A.R., and McCulloch, M.T., 1991a. Coprecipitation and isotopic fractionation of boron in modern biogenic carbonates. Geochim. Cosmochim. Acta 55, pp. 2901–2910.
Vengosh, A., Starinsky, A., Kolodny, Y., and Chivas, A.R., 1991b. Boron-isotope geochemistry as a tracer for the evolution of brines and associated hot springs from the Dead Sea, Israel. Geochim. Cosmochim. Acta 55, pp. 1689–1695.
Vengosh, A., Starinsky, A., Kolodny, Y., Chivas, A.R., and Raab, M., 1992. Boron isotope variations during fractional evaporation of sea water: new constraints on the marine vs. nonmarine debate. Geology 20, pp. 799–802.
Vengosh, A., 2003. Salinization and Saline Environments. In: Sherwood Lollar, B. (ed.), Environmental geochemistry (volume 9), Treatise in Geochemistry. Executive Editors: Holland, H.D. and Turekian, K.T., Elsevier Science.
Waldmann, N., 2002. The geology of the Samra Formation in the Dead Sea Basin. M.Sc. Thesis, The Hebrew University of Jerusalem, Israel.
Williams, W.D., 2001. Anthropogenic salinization of inland waters. J. Hydrobiol. 466, pp. 329–337.
Yechieli, Y., Gavrieli, I., Berkowitz, B., and Ronen, D., 1998. Will the Dead Sea die? Geology 26, pp. 755–758.
Zak, I., 1967. The geology of Mount Sedom. Unpubl. Ph.D. Thesis, The Hebrew University of Jerusalem (in Hebrew with English abstract).
Zak, I., 1997. Evolution of the Dead Sea brines. In: Niemi, T.M., Ben-Avraham, Z. and Gat, J.R., Editors, 1997. The Dead Sea, The Lake and Its Setting. Oxford Monograph on Geology and Geophysics. 36. 133–144.
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The Lower Jordan River: River Salinization, Relationship with Adjacent Groundwater and Future Management
Appendix I- Analytical results
By Efrat Farber
Submitted to the Senate of Ben-Gurion University of the Negev
110 11 87 86 ID name E x N yDistance from Date Conductivity Temp pH D.O δ B Sr/ Sr River Alumot (km) m.s oC ‰ JR-007 Alumot Bridge 253.0 734.1 0.1 9/1/1999 8.15 31.6 7.40 4.50 29.20 0.70775 JR-26 Alumot Bridge 253.0 734.1 0.1 3/30/2000 8.59 25.5 7.30 JR-70 Alumot Bridge 253.0 734.1 0.1 5/24/2000 29.4 7.80 30.47 0.70774 JR-92 Alumot Bridge 253.0 734.1 0.1 8/8/2000 8.64 31.9 7.20 32.80 0.70779 JR-106 Alumot Bridge 253.0 734.1 0.1 9/25/2000 8.37 30.4 7.50 32.22 0.70776 JR-117 Alumot Bridge 253.0 734.1 0.1 12/17/2000 7.30 19.7 7.39 JR-147 Alumot Bridge 253.0 734.1 0.1 2/28/2001 6.46 24.6 7.33 3.90 JR-178 Alumot Bridge 253.0 734.1 0.1 3/29/2001 6.74 24.4 7.28 0.88 JR-223 Alumot Bridge 253.0 734.1 0.1 4/22/2001 6.81 28.1 7.23 1.50 JR-251 Alumot Bridge 253.0 734.1 0.1 6/10/2001 6.29 24.3 7.18 0.81 JR-281 Alumot Bridge 253.0 734.1 0.1 8/3/2001 7.17 26.9 6.78 1.12 JR-27 Beit Zera 253.6 732.9 1.3 3/30/2000 7.01 25.0 7.40 JR-69 Beit Zera 253.6 732.9 1.3 5/24/2000 30.3 7.90 33.47 0.70776 JR-93 Beit Zera 253.6 732.9 1.3 8/8/2000 8.76 33.3 7.30 JR-108 Beit Zera 253.6 732.9 1.3 9/25/2000 8.53 30.1 7.40 32.47 0.70776 JR-116 Beit Zera 253.6 732.9 1.3 12/17/2000 6.20 17.8 7.40 JR-145 Beit Zera 253.6 732.9 1.3 2/28/2001 7.02 25.0 7.30 2.00 JR-177 Beit Zera 253.6 732.9 1.3 3/29/2001 7.30 25.7 7.41 1.76 JR-221 Beit Zera 253.6 732.9 1.3 4/22/2001 6.68 27.9 7.45 2.94 JR-253 Beit Zera 253.6 732.9 1.3 6/10/2001 6.00 23.0 7.35 1.83 JR-283 Beit Zera 253.6 732.9 1.3 8/3/2001 6.40 26.2 7.00 1.35 JR-341 Beit Zera 253.6 732.9 1.3 8/12/2001 JR-366 Beit Zera 253.6 732.9 1.3 1/3/2002 6.08 19.2 7.02 3.63 JR-367 Beit-Zera Up 253.6 733.2 1.0 1/3/2002 6.04 19.4 6.98 3.36 JR-365 Ubadia 253.6 731.9 2.3 1/3/2002 6.23 18.3 7.00 3.51 JR-358 Menahamia 252.7 731.0 3.2 1/3/2002 JR-006 Dalhamiya Bridge 253.8 728.6 5.6 9/1/1999 7.90 32.5 7.90 8.20 30.50 0.70774 JR-23 Dalhamiya Bridge 253.8 728.6 5.6 3/30/2000 6.86 22.5 7.60 JR-68 Dalhamiya Bridge 253.8 728.6 5.6 5/24/2000 29.2 8.00 32.22 0.70776 JR-91 Dalhamiya Bridge 253.8 728.6 5.6 8/8/2000 8.65 33.8 7.20 31.60 0.70773 JR-144 Dalhamiya Bridge 253.8 728.6 5.6 2/28/2001 6.75 23.2 7.46 2.81 JR-176 Dalhamiya Bridge 253.8 728.6 5.6 3/29/2001 6.57 25.0 7.52 2.60 JR-220 Dalhamiya Bridge 253.8 728.6 5.6 4/22/2001 6.96 26.2 7.52 4.53 11 87 86 ID name E x N yDistance from Date Conductivity Temp pH D.O δ B Sr/ Sr River (Continued) Alumot (km) m.s oC ‰ JR-254 Dalhamiya Bridge 253.8 728.6 5.6 6/10/2001 6.63 24.2 7.53 4.03 JR-304 Dalhamiya Bridge 253.8 728.6 5.6 8/3/2001 6.71 27.6 7.16 2.11 JR-340 Dalhamiya Bridge 253.8 728.6 5.6 8/12/2001 JR-360 Dalhamiya Bridge 253.8 728.6 5.6 1/3/2002 6.53 16.6 6.45 3.94 JR-455 Dalhamiya Bridge 253.8 728.6 6.0 2/3/2004 6.05 16.8 7.41 3.51 JR-24 Naharayim 253.1 726.9 7.3 3/30/2000 6.75 21.4 7.40 JR-66 Naharayim 253.1 726.9 7.3 5/24/2000 5.25 25.9 8.40 JR-89 Gesher 253.2 725.5 8.7 8/8/2000 8.68 32.0 7.30 33.50 0.70773 JR-114 Gesher 253.2 725.5 8.7 12/17/2000 6.30 14.4 7.62 JR-142 Gesher 253.2 725.5 8.7 2/28/2001 6.78 20.2 7.25 2.73 JR-174 Gesher 253.2 725.5 8.7 3/29/2001 7.04 24.9 7.46 2.70 JR-218 Gesher 253.2 725.5 8.7 4/22/2001 7.15 25.3 7.41 2.65 JR-256 Gesher 253.2 725.5 8.7 6/10/2001 6.88 25.5 7.50 3.40 JR-284 Gesher 253.2 725.5 8.7 8/3/2001 6.94 30.6 7.21 3.05 JR-363 Gesher 253.2 725.5 8.7 1/3/2002 6.68 15.8 7.12 3.56 JR-21 N.Ur north (78) 253.5 722.7 11.6 3/30/2000 6.15 20.6 7.70 JR-64 N.Ur north (78) 253.5 722.7 11.6 5/24/2000 7.38 26.7 8.00 33.97 0.70765 JR-94 N.Ur north (78) 253.5 722.7 11.6 8/8/2000 8.72 32.1 7.50 34.80 0.70764 JR-105 N.Ur north (78) 253.5 722.7 11.6 9/25/2000 31.72 0.70762 JR-112 N.Ur north (78) 253.5 722.7 11.6 12/17/2000 6.30 12.9 8.02 JR-141 N.Ur north (78) 253.5 722.7 11.6 2/28/2001 6.72 19.2 7.52 6.18 JR-171 N.Ur north (78) 253.5 722.7 11.6 3/29/2001 6.92 24.7 7.52 3.63 JR-214 N.Ur north (78) 253.5 722.7 11.6 4/23/2001 7.09 27.6 7.47 3.69 JR-259 N.Ur north (78) 253.5 722.7 11.6 6/10/2001 6.69 25.0 7.42 3.05 JR-288 N.Ur north (78) 253.5 722.7 11.6 8/3/2001 7.14 29.8 7.35 3.59 JR-364 N.Ur north (78) 253.5 722.7 11.6 1/3/2002 6.56 15.6 7.14 5.03 JR-504 N.Ur north (78) 253.5 722.7 11.6 10/15/2003 JR-464 N.Ur north (78) 253.5 722.7 11.6 3/10/2004 4.13 19.5 7.29 7.10 Jk-36 N.Ur north (78-pump) 253.5 722.7 11.6 10/26/2004 6.11 24.2 6.56 9.33 Jk-37 N.Ur north (78-river) 253.5 722.7 11.6 10/26/2004 6.70 23.8 7.01 9.50 JK-62 N.Ur north (78) 253.5 722.7 11.6 2/22/2005 4.29 19.6 6.90 6.77 JR-22 N.Ur south (74) 254.4 721.5 12.7 3/30/2000 5.88 20.9 7.70 JR-65 N.Ur south (74) 254.4 721.5 12.7 5/24/2000 6.20 25.0 8.10 30.47 0.70765 11 87 86 ID name E x N yDistance from Date Conductivity Temp pH D.O δ B Sr/ Sr River (Continued) Alumot (km) m.s oC ‰ JR-96 N.Ur south (74) 254.4 721.5 12.7 8/8/2000 7.24 31.9 7.60 32.30 0.70762 JR-104 N.Ur south (74) 254.4 721.5 12.7 9/25/2000 31.72 0.70759 JR-113 N.Ur south (74) 254.4 721.5 12.7 12/17/2000 5.80 13.7 7.94 JR-140 N.Ur south (74) 254.4 721.5 12.7 2/28/2001 6.01 19.7 7.45 5.42 JR-170 N.Ur south (74) 254.4 721.5 12.7 3/29/2001 6.34 24.3 7.65 6.63 JR-212 N.Ur south (74) 254.4 721.5 12.7 4/22/2001 5.85 24.0 7.20 2.20 JR-261 N.Ur south (74) 254.4 721.5 12.7 6/10/2001 6.06 25.0 7.60 4.20 JR-291 N.Ur south (74) 254.4 721.5 12.7 8/3/2001 6.41 28.5 7.45 4.86 JR-503 N.Ur south (74) 254.4 721.5 12.7 10/15/2003 JR-508 N.Ur south (74) 254.4 721.5 12.7 6/23/2004 JR-502 N.Ur south (74) 254.4 721.5 12.7 10/15/2003 JR-463 N.Ur south (74) 254.4 721.5 12.7 3/10/2004 4.03 18.2 7.24 7.43 JK-63 N.Ur south (74) 254.4 721.5 12.7 2/22/2005 Jk-38 N.Ur south (74) 254.4 721.5 12.7 10/26/2004 6.71 23.3 6.93 7.61 JR-462 Gimel 73 13.2 3/10/2004 3.98 18.0 7.15 7.00 JR-507 Gimel 73 13.2 6/23/2004 Jk-35 Gimel 73 13.2 10/26/2004 5.98 23.3 6.55 4.90 JK-64 Gimel 73 13.2 2/22/2005 JR-18 Hamadiya North (56) 253.0 715.6 18.6 3/30/2000 5.50 20.1 7.50 JR-63 Hamadiya North (56) 253.0 715.6 18.6 5/24/2000 25.5 7.90 30.22 JR-169 Hamadiya North (56) 252.8 715.8 18.4 3/29/2001 6.40 22.9 7.77 3.60 JR-210 Hamadiya North (56) 253.0 715.6 18.6 4/22/2001 6.12 23.8 7.49 4.24 JR-262 Hamadiya North (56) 253.0 715.6 18.6 6/10/2001 6.13 25.6 7.80 5.03 JR-292 Hamadiya North (56) 253.0 715.6 18.6 8/3/2001 5.95 29.0 7.68 5.01 JR-500 Hamadiya North (56) 253.0 715.6 18.6 10/15/2003 JR-461 Hamadiya North (56) 253.0 715.6 18.6 3/10/2004 4.31 17.8 7.16 7.41 JR-505 Hamadiya North (56) 253.0 715.6 18.6 6/23/2004 Jk-34 Hamadiya North (56) 253.0 715.6 18.6 10/26/2004 6.15 22.8 7.24 6.80 JK-59 Hamadiya North (56) 253.0 715.6 18.6 2/22/2005 4.49 17.6 6.56 2.53 JR-509 Shaar 58 6/23/2004 JR-501 Canal 56 gimel 19.5 10/15/2003 JR-460 Canal 56 gimel 19.5 3/10/2004 4.31 17.8 6.89 5.74 JR-506 Canal 56 gimel 19.5 6/23/2004 11 87 86 ID name E x N yDistance from Date Conductivity Temp pH D.O δ B Sr/ Sr River (Continued) Alumot (km) m.s oC ‰ Jk-33 Canal 56 gimel 19.5 10/26/2004 6.22 22.8 7.04 3.41 JK-56 Canal 56 gimel 19.5 2/22/2005 3.18 16.0 6.77 5.87 JR-20 Hamadiya South (Zor) 252.7 714.1 20.1 3/30/2000 5.50 20.2 7.70 JR-62 Hamadiya South (Zor) 252.7 714.1 20.1 5/24/2000 26.3 8.50 30.47 0.70766 JR-88 Hamadiya South (Zor) 252.7 714.1 20.1 8/8/2000 6.90 30.3 7.40 JR-111 Hamadiya South (Zor) 252.7 714.1 20.1 12/17/2000 5.50 12.6 8.05 JR-139 Hamadiya South (Zor) 252.7 714.1 20.1 2/28/2001 5.83 19.2 7.38 5.55 JR-165 Hamadiya South (Zor) 252.7 714.1 20.1 3/29/2001 6.02 23.7 7.55 3.93 JR-209 Hamadiya South (Zor) 252.7 714.1 20.1 4/22/2001 6.15 23.9 7.49 3.47 JR-263 Hamadiya South (Zor) 252.7 714.1 20.1 6/10/2001 6.28 26.4 7.93 6.85 JR-294 Hamadiya South (Zor) 252.7 714.1 20.1 8/3/2001 6.01 28.8 7.64 4.50 JR-162 g-48 252.6 713.2 21.1 3/29/2001 6.21 22.5 7.56 2.30 JR-204 g-48 252.6 713.2 21.1 4/23/2001 6.11 23.4 7.57 3.90 JR-269 g-48 252.6 713.2 21.1 6/10/2001 6.02 27.3 7.69 4.31 JR-298 g-48 252.6 713.2 21.1 8/3/2001 6.30 26.7 7.51 1.40 JR-16 Maoz Haim 253.3 712.0 22.2 3/30/2000 5.52 19.5 7.70 JR-57 Maoz Haim 253.3 712.0 22.2 5/24/2000 6.20 23.9 8.20 32.72 0.70763 JR-137 Maoz Haim 253.3 712.0 22.2 2/28/2001 5.90 18.4 7.49 1.63 JR-161 Maoz Haim 253.3 712.0 22.2 3/29/2001 6.01 23.1 7.65 4.08 JR-203 Maoz Haim 253.3 712.0 22.2 4/23/2001 5.99 23.8 7.62 4.40 JR-270 Maoz Haim 253.3 712.0 22.2 6/10/2001 5.97 29.3 8.09 10.32 JR-300 Maoz Haim 253.3 712.0 22.2 8/3/2001 6.19 27.6 7.47 1.72 JR-013 Sheich Husein Bridge 254.4 711.5 22.7 9/11/1999 JR-15 Sheich Husein Bridge 254.4 711.5 22.7 3/30/2000 5.08 19.6 7.50 JR-53 Sheich Husein Bridge 254.4 711.5 22.7 5/24/2000 6.35 23.7 8.10 32.72 0.70767 JR-135 Sheich Husein Bridge 254.4 711.5 22.7 2/28/2001 5.65 17.6 7.53 2.18 JR-159 Sheich Husein Bridge 254.4 711.5 22.7 3/29/2001 6.14 21.2 7.99 8.99 JR-201 Sheich Husein Bridge 254.4 711.5 22.7 4/22/2001 5.91 23.1 7.61 4.82 JR-272 Sheich Husein Bridge 254.4 711.5 22.7 6/10/2001 6.03 26.3 7.93 7.58 JR-302 Sheich Husein Bridge 254.4 711.5 22.7 8/3/2001 5.87 27.5 7.49 4.64 JR-339 Sheich Husein Bridge 254.4 711.5 22.7 8/12/2001 JR-414 Sheich Husein Bridge 254.4 711.5 22.7 2/23/2003 470.00 0.70713 JR-422 Sheich Husein Bridge 254.4 711.5 22.7 3/17/2003 1.93 14.4 8.13 0.70741 11 87 86 ID name E x N yDistance from Date Conductivity Temp pH D.O δ B Sr/ Sr River (Continued) Alumot (km) m.s oC ‰ JR-453 Sheich Husein Bridge 254.4 711.5 22.7 2/3/2004 1.00 13.9 7.58 7.68 JR-004 Shifa' Station 253.5 706.5 27.7 9/1/1999 5.73 30.8 7.60 7.50 31.50 0.70771 JR-14 Shifa' Station 253.5 706.5 27.7 3/30/2000 4.93 18.8 7.90 JR-54 Shifa' Station 253.5 706.5 27.7 5/24/2000 6.23 24.3 8.20 32.97 0.70770 JR-84 Shifa' Station 253.5 706.5 27.7 8/8/2000 6.75 28.4 7.60 33.80 0.70770 JR-110 Shifa' Station 253.5 706.5 27.7 12/17/2000 5.10 11.9 8.16 JR-134 Shifa' Station 253.5 706.5 27.7 2/28/2001 5.66 16.6 7.42 JR-158 Shifa' Station 253.5 706.5 27.7 3/29/2001 6.40 20.6 7.62 3.84 JR-200 Shifa' Station 253.5 706.5 27.7 4/22/2001 6.05 23.4 7.48 3.65 JR-273 Shifa' Station 253.5 706.5 27.7 6/10/2001 6.09 24.6 7.53 5.08 JR-303 Shifa' Station 253.5 706.5 27.7 8/3/2001 6.05 27.6 7.14 2.33 JR-11 Gibton 253.0 690.2 44.0 3/29/2000 4.95 19.7 8.30 JR-50 Gibton 253.0 690.2 44.0 5/23/2000 26.3 8.90 36.71 0.70785 JR-82 Gibton 253.0 690.2 44.0 8/7/2000 6.80 31.9 7.70 JR-157 Gibton 253.0 690.2 44.0 3/28/2001 5.64 22.9 8.08 8.26 JR-246 Gibton 253.0 690.2 44.0 6/4/2001 5.50 29.4 8.70 16.00 JR-81 Zarzir Station-58 254.0 674.5 59.7 8/7/2000 6.66 31.2 7.30 32.60 0.70797 JR-103 Zarzir Station-58 254.0 674.5 59.7 9/25/2000 32.47 0.70788 JR-131 Zarzir Station-58 254.0 674.5 59.7 2/27/2001 5.24 18.8 7.88 7.70 34.47 0.70790 JR-156 Zarzir Station-58 254.0 674.5 59.7 3/28/2001 5.80 24.2 8.35 14.56 JR-183 Zarzir Station-58 254.0 674.5 59.7 4/11/2001 JR-234 Zarzir Station-58 254.0 674.5 59.7 4/23/2001 6.20 24.1 7.84 5.10 JR-245 Zarzir Station-58 254.0 674.5 59.7 6/4/2001 5.30 28.0 7.98 2.31 JR-337 Zarzir Station-58 254.0 674.5 59.7 8/12/2001 JR-370 Zarzir Station-58 254.0 674.5 59.7 7/2/2002 6.92 31.3 8.13 JR-406 Zarzir Station-58 254.0 674.5 59.7 8/27/2002 6.50 26.9 8.07 JR-421 Zarzir Station-58 254.0 674.5 59.7 3/17/2003 1.80 0.70754 JR-428 Zarzir Station-58 254.0 674.5 59.7 6/16/2003 JR-003 Adam Bridge 250.5 667.8 66.4 9/1/1999 5.88 30.2 7.70 8.50 31.00 0.70829 JR-010 Adam Bridge 250.5 667.8 66.4 9/11/1999 JR-9 Adam Bridge 250.5 667.8 66.4 3/29/2000 5.39 20.2 8.20 JR-49 Adam Bridge 250.5 667.8 66.4 5/23/2000 26.3 8.80 30.97 0.70815 JR-80 Adam Bridge 250.5 667.8 66.4 8/7/2000 6.96 31.4 7.80 30.70 0.70810 11 87 86 ID name E x N yDistance from Date Conductivity Temp pH D.O δ B Sr/ Sr River (Continued) Alumot (km) m.s oC ‰ JR-102 Adam Bridge 250.5 667.8 66.4 9/25/2000 30.47 0.70806 JR-130 Adam Bridge 250.5 667.8 66.4 2/27/2001 5.37 18.6 7.94 7.87 33.47 0.70803 JR-155 Adam Bridge 250.5 667.8 66.4 3/28/2001 6.40 23.0 8.40 14.90 JR-233 Adam Bridge 250.5 667.8 66.4 4/23/2001 7.06 23.9 7.94 10.00 JR-244 Adam Bridge 250.5 667.8 66.4 6/4/2001 5.48 29.5 8.57 13.00 JR-336 Adam Bridge 250.5 667.8 66.4 8/12/2001 6.70 32.3 8.07 8.42 JR-371 Adam Bridge 250.5 667.8 66.4 7/2/2002 6.77 30.5 7.35 9.85 JR-405 Adam Bridge 250.5 667.8 66.4 8/27/2002 7.20 25.7 7.87 JR-410 Adam Bridge 250.5 667.8 66.4 12/18/2002 3.95 10.6 7.00 JR-412 Adam Bridge 250.5 667.8 66.4 2/23/2003 0.63 7.73 0.70759 JR-420 Adam Bridge 250.5 667.8 66.4 3/17/2003 2.15 14.4 8.16 0.70773 JR-452 Adam Bridge 250.5 667.8 66.4 2/3/2004 JR-8 Tovlan Station -83 249.1 661.8 72.4 3/29/2000 5.85 19.6 8.40 JR-47 Tovlan Station -83 249.1 661.8 72.4 5/23/2000 25.0 8.60 32.72 0.70818 JR-79 Tovlan Station -83 249.1 661.8 72.4 8/7/2000 8.13 30.4 7.60 JR-100 Tovlan Station -83 249.1 661.8 72.4 9/25/2000 7.32 27.8 7.80 29.97 0.70805 JR-126 Tovlan Station -83 249.1 661.8 72.4 2/27/2001 6.17 18.1 7.90 7.95 31.97 0.70804 JR-154 Tovlan Station -83 249.1 661.8 72.4 3/28/2001 7.20 21.7 8.16 9.73 JR-231 Tovlan Station -83 249.1 661.8 72.4 4/23/2001 9.30 24.0 7.86 6.65 JR-242 Tovlan Station -83 249.1 661.8 72.4 6/4/2001 6.21 28.2 8.18 9.30 JR-335 Tovlan Station -83 249.1 661.8 72.4 8/12/2001 8.05 31.1 8.03 5.91 JR-375 Tovlan Station -83 249.1 661.8 72.4 7/2/2002 7.30 30.8 7.51 4.57 JR-404 Tovlan Station -83 249.1 661.8 72.4 8/27/2002 7.70 26.0 7.70 JR-413 Tovlan Station -83 249.1 661.8 72.4 2/23/2003 0.71 0.70773 JR-427 Tovlan Station -83 249.1 661.8 72.4 6/16/2003 JK-48 Tovlan Station -83 249.1 661.8 72.4 11/15/2004 6.50 23.0 7.20 6.40 JK-55 Tovlan Station -83 249.1 661.8 72.4 1/26/2005 JK-77 Tovlan Station -83 249.1 661.8 72.4 4/26/2005 JR-5 Gilgal - 107 249.9 657.6 76.6 3/29/2000 6.05 20.0 8.10 JR-45 Gilgal - 107 249.9 657.6 76.6 5/23/2000 24.0 8.50 32.97 0.70814 JR-78 Gilgal - 107 249.9 657.6 76.6 8/7/2000 7.94 29.7 7.60 JR-153 Gilgal - 107 249.9 657.6 76.6 3/28/2001 7.13 21.4 8.12 9.35 JR-230 Gilgal - 107 249.9 657.6 76.6 4/23/2001 9.30 23.5 7.87 8.33 11 87 86 ID name E x N yDistance from Date Conductivity Temp pH D.O δ B Sr/ Sr River (Continued) Alumot (km) m.s oC ‰ JR-240 Gilgal - 107 249.9 657.6 76.6 6/4/2001 5.80 28.2 8.30 6.95 JR-334 Gilgal - 107 249.9 657.6 76.6 8/12/2001 9.10 30.5 7.88 5.14 JR-403 Gilgal - 107 249.9 657.6 76.6 8/27/2002 JK-45 Gilgal - 107 249.9 657.6 76.6 11/15/2004 6.50 23.0 7.10 6.00 JK-54 Gilgal - 107 249.9 657.6 76.6 1/26/2005 JK-76 Gilgal - 107 249.9 657.6 76.6 4/26/2005 JR-44 Zur el mandase 251.5 649.6 84.6 5/23/2000 23.3 8.10 31.72 0.70807 JR-002 Alenby Bridge 251.2 642.8 91.4 9/1/1999 7.88 28.9 8.30 30.70 0.70820 JR-011 Alenby Bridge 251.2 642.8 91.4 9/11/1999 JR-3 Alenby Bridge 251.2 642.8 91.4 3/29/2000 6.13 19.7 8.00 JR-42 Alenby Bridge 251.2 642.8 91.4 5/23/2000 24.2 8.20 31.72 0.70809 JR-76 Alenby Bridge 251.2 642.8 91.4 8/7/2000 8.37 29.9 7.20 31.70 0.70807 JR-97 Alenby Bridge 251.2 642.8 91.4 9/25/2000 6.80 25.5 7.50 30.22 0.70806 JR-124 Alenby Bridge 251.2 642.8 91.4 2/27/2001 6.66 16.4 7.70 8.30 JR-152 Alenby Bridge 251.2 642.8 91.4 3/28/2001 10.00 20.9 8.00 7.12 JR-228 Alenby Bridge 251.2 642.8 91.4 4/23/2001 8.34 22.9 7.68 5.53 JR-239 Alenby Bridge 251.2 642.8 91.4 6/4/2001 9.70 28.1 8.00 4.71 JR-332 Alenby Bridge 251.2 642.8 91.4 8/12/2001 12.30 30.3 7.58 4.71 JR-372 Alenby Bridge 251.2 642.8 91.4 7/2/2002 8.13 31.6 7.88 7.57 JR-402 Alenby Bridge 251.2 642.8 91.4 8/27/2002 10.80 24.5 7.72 JR-409 Alenby Bridge 251.2 642.8 91.4 12/18/2002 4.72 10.4 7.21 JR-419 Alenby Bridge 251.2 642.8 91.4 3/17/2003 1.87 13.5 8.35 0.70768 JR-451 Alenby Bridge 251.2 642.8 91.4 2/3/2004 14.0 7.80 JR-001 Baptism site 251.8 638.6 95.6 9/1/1999 8.13 28.6 7.70 5.80 31.00 0.70813 JR-012 Baptism site 251.8 638.6 95.6 9/11/1999 JR-2 Baptism site 251.8 638.6 95.6 3/29/2000 6.01 18.6 8.00 JR-75 Baptism site 251.8 638.6 95.6 8/7/2000 9.07 29.6 7.10 31.60 0.70816 JR-98 Baptism site 251.8 638.6 95.6 9/25/2000 7.22 26.0 7.10 29.72 0.70808 JR-122 Baptism site 251.8 638.6 95.6 2/27/2001 6.70 15.2 7.37 9.36 JR-151 Baptism site 251.8 638.6 95.6 3/28/2001 9.80 19.9 7.64 5.74 JR-227 Baptism site 251.8 638.6 95.6 4/23/2001 9.10 23.0 7.71 5.46 JR-238 Baptism site 251.8 638.6 95.6 6/4/2001 10.60 27.2 7.87 3.84 JR-331 Baptism site 251.8 638.6 95.6 8/12/2001 15.40 31.2 7.44 3.11 11 87 86 ID name E x N yDistance from Date Conductivity Temp pH D.O δ B Sr/ Sr River (Continued) Alumot (km) m.s oC ‰ JR-373 Baptism site 251.8 638.6 95.6 7/2/2002 9.10 30.3 7.88 9.97 JR-401 Baptism site 251.8 638.6 95.6 8/27/2002 11.30 24.5 7.68 JR-408 Baptism site 251.8 638.6 95.6 12/18/2002 6.90 9.3 7.87 JR-411 Baptism site 251.8 638.6 95.6 2/23/2003 1.79 7.90 0.70781 JR-418 Baptism site 251.8 638.6 95.6 3/17/2003 1.90 14.1 8.06 0.70772 JR-426 Baptism site 251.8 638.6 95.6 6/16/2003 JR-99 Ab'dala Bridge 251.8 634.2 100.0 9/25/2000 7.47 27.1 7.10 30.22 0.70805 JR-123 Ab'dala Bridge 251.8 634.2 100.0 2/27/2001 6.08 15.5 7.79 8.47 JR-150 Ab'dala Bridge 251.8 634.2 100.0 3/28/2001 9.50 20.2 7.87 6.79 JR-226 Ab'dala Bridge 251.8 634.2 100.0 4/23/2001 8.41 22.8 7.67 6.50 JR-237 Ab'dala Bridge 251.8 634.2 100.0 6/4/2001 11.50 27.3 7.97 4.85 JR-330 Ab'dala Bridge 251.8 634.2 100.0 8/12/2001 16.90 30.3 7.36 3.93 JR-374 Ab'dala Bridge 251.8 634.2 100.0 7/2/2002 8.78 30.6 7.89 12.90 JR-400 Ab'dala Bridge 251.8 634.2 100.0 8/27/2002 11.40 25.0 7.58 JR-407 Ab'dala Bridge 251.8 634.2 100.0 12/18/2002 6.02 9.4 8.72 JR-417 Ab'dala Bridge 251.8 634.2 100.0 3/17/2003 1.80 13.1 8.17 0.70773 JR-425 Ab'dala Bridge 251.8 634.2 100.0 6/16/2003 Western inflows JR-118 Bitaniya 253.0 734.2 0.0 12/17/2000 2.40 14.7 7.65 JR-148 Bitaniya 253.0 734.2 0.0 2/28/2001 JR-180 Bitaniya 253.0 734.2 0.0 3/29/2001 2.79 22.2 7.62 2.20 JR-225 Bitaniya 253.0 734.2 0.0 4/22/2001 2.77 25.0 7.59 2.35 JR-249 Bitaniya 253.0 734.2 0.0 6/9/2001 2.78 24.1 7.52 2.23 JR-280 Bitaniya 253.0 734.2 0.0 8/3/2001 2.72 27.3 6.84 2.20 JR-342 Bitaniya 253.0 734.2 0.0 8/12/2001 JR-351 Bitaniya 253.0 734.2 0.0 1/3/2002 JR-107 Saline carrier 253.0 734.2 0.0 9/25/2000 31.97 0.70774 JR-119 Saline carrier 253.0 734.2 0.0 12/17/2000 8.60 20.8 7.50 JR-149 Saline carrier 253.0 734.2 0.0 2/28/2001 9.30 25.3 7.24 3.20 JR-179 Saline carrier 253.0 734.2 0.0 3/29/2001 7.11 24.9 7.20 1.55 JR-224 Saline carrier 253.0 734.2 0.0 4/22/2001 7.47 28.1 7.37 3.46 JR-250 Saline carrier 253.0 734.2 0.0 6/9/2001 6.63 24.2 7.08 2.50 JR-279 Saline carrier 253.0 734.2 0.0 8/3/2001 7.55 26.8 6.66 2.30 11 87 86 ID name E x N y Date Conductivity Temp pH D.O δ B Sr/ Sr Western inflows (Continued) m.s oC ‰ JR-343 Saline carrier 253.0 734.2 0.0 8/12/2001 JR-350 Saline carrier 253.0 734.2 0.0 1/3/2002 JR-146 W. Yavneal 252.8 733.8 0.4 2/28/2001 1.51 21.0 8.12 6.60 JR-181 W. Yavneal 252.8 733.8 0.4 3/29/2001 1.48 19.8 8.16 6.23 JR-222 W. Yavneal 252.8 733.8 0.4 4/23/2001 1.44 23.1 8.02 5.30 JR-252 W. Yavneal 252.8 733.8 0.4 6/9/2001 1.40 20.9 7.91 5.98 JR-282 W. Yavneal 252.8 733.8 0.4 8/3/2001 1.41 23.7 7.25 5.02 JR-188 point 110 256.7 730.5 3.7 4/12/2001 JR-187 point 121 259.0 731.6 2.6 4/12/2001 30.47 0.70752 JR-344 point 121 259.0 731.6 2.6 8/12/2001 JR-368 point 121 259.0 731.6 2.6 1/3/2002 1.03 19.8 7.81 8.25 31.80 0.70754 JR-185 Yarmuhim Reseruoir 257.2 730.9 3.3 4/12/2001 JR-359 Yarmuhim Reseruoir 257.2 730.9 3.3 1/3/2002 32.80 0.70758 JR-005 Yarmuok River - Naharayim 254.1 727.9 6.3 9/1/1999 5.05 30.4 7.80 8.70 36.20 0.70719 JR-25 Yarmuok River - Naharayim 254.1 727.9 6.3 3/30/2000 4.34 21.5 8.20 JR-67 Yarmuok River - Naharayim 254.1 727.9 6.3 5/24/2000 36.71 0.70716 JR-90 Yarmuok River - Naharayim 254.1 727.9 6.3 8/8/2000 6.49 31.1 7.20 JR-115 Yarmuok River - Naharayim 254.1 727.9 6.3 12/17/2000 4.20 13.2 8.37 JR-143 Yarmuok River - Naharayim 254.1 727.9 6.3 2/28/2001 4.11 19.2 8.00 9.10 JR-175 Yarmuok River - Naharayim 254.1 727.9 6.3 3/29/2001 5.78 22.5 8.18 8.28 JR-198 Yarmuok River - Naharayim 254.1 727.9 6.3 4/12/2001 JR-219 Yarmuok River - Naharayim 254.1 727.9 6.3 4/23/2001 5.35 23.7 8.13 7.60 JR-255 Yarmuok River - Naharayim 254.1 727.9 6.3 6/9/2001 6.36 26.9 8.02 6.28 JR-285 Yarmuok River - Naharayim 254.1 727.9 6.3 8/3/2001 12.30 29.6 7.60 10.00 JR-361 Yarmuok River - Naharayim 254.1 727.9 6.3 1/3/2002 4.98 15.3 7.55 9.05 JR-415 Yarmuok River - Naharayim 254.1 727.9 6.3 2/23/2003 417.00 0.70693 JR-423 Yarmuok River - Naharayim 254.1 727.9 6.3 3/17/2003 1.04 14.6 8.05 0.70714 JR-454 Yarmuok River - Naharayim 254.1 727.9 6.3 2/3/2004 0.48 13.6 7.95 9.84 JR-173 Gesher drainage (81) 253.8 723.5 10.7 3/29/2001 6.58 27.5 7.63 2.55 JR-217 Gesher drainage (81) 253.8 723.5 10.7 4/23/2001 6.52 25.0 7.56 3.30 JR-257 Gesher drainage (81) 253.8 723.5 10.7 6/9/2001 6.04 24.0 7.87 4.17 JR-286 Gesher drainage (81) 253.8 723.5 10.7 8/3/2001 9.10 30.2 7.31 3.48 JR-172 N.Ur - Water canal (78) 253.4 722.7 11.5 3/29/2001 7.67 22.5 7.87 4.90 11 87 86 ID name E x N y Date Conductivity Temp pH D.O δ B Sr/ Sr Western inflows (Continued) m.s oC ‰ JR-215 N.Ur - Water canal (78) 253.4 722.7 11.5 4/22/2001 7.40 22.6 7.68 4.87 JR-258 N.Ur - Water canal (78) 253.4 722.7 11.5 6/9/2001 7.01 25.0 7.60 4.30 JR-287 N.Ur - Water canal (78) 253.4 722.7 11.5 8/3/2001 7.62 27.0 7.20 1.45 JR-213 N.Ur - Water canal (76) 254.4 722.0 12.2 4/23/2001 7.05 22.0 7.36 3.26 JR-260 N.Ur - Water canal (76) 254.4 722.0 12.2 6/9/2001 7.24 24.9 7.40 3.30 JR-290 N.Ur - Water canal (74) 254.4 721.5 12.7 8/3/2001 6.80 29.9 7.70 4.06 JR-168 Hamadiya - south canal 252.7 715.3 18.9 3/29/2001 6.43 25.1 7.91 7.70 JR-207 Hamadiya - south canal 252.7 715.3 18.9 4/23/2001 5.96 23.2 7.84 8.65 JR-264 Hamadiya - south canal 252.7 715.3 18.9 6/9/2001 6.43 25.0 7.47 3.71 JR-295 Hamadiya - south canal 252.7 715.3 18.9 8/3/2001 6.79 25.8 7.20 2.40 JR-17 W. Harod 251.8 713.5 20.8 3/29/2000 5.52 20.4 7.70 JR-60 W. Harod 251.8 713.5 20.8 5/24/2000 6.46 24.0 8.10 39.46 0.70782 JR-85 W. Harod 251.8 713.5 20.8 8/8/2000 6.87 25.1 7.50 JR-138 W. Harod 251.8 713.5 20.8 2/28/2001 5.82 19.7 7.42 4.00 JR-164 W. Harod 251.8 713.5 20.8 3/29/2001 5.81 22.7 7.57 2.94 JR-206 W. Harod 251.8 713.5 20.8 4/23/2001 5.83 21.6 7.36 1.90 JR-267 W. Harod 251.8 713.5 20.8 6/9/2001 5.49 25.0 7.41 3.16 JR-297 W. Harod 251.8 713.5 20.8 8/3/2001 5.74 24.9 7.45 1.21 JR-59 Water canal 48 252.1 712.8 21.4 5/24/2000 7.80 21.4 8.40 38.21 0.70792 JR-163 Water canal 48 252.1 712.8 21.4 3/29/2001 6.72 20.0 7.72 5.34 JR-205 Water canal 48 252.1 712.8 21.4 4/22/2001 7.62 17.8 7.66 5.86 JR-268 Water canal 48 252.1 712.8 21.4 6/9/2001 6.16 25.4 7.79 5.10 JR-16 Water canal Nimrod 253.3 712.0 22.2 3/30/2000 JR-58 Water canal Nimrod 253.3 712.0 22.2 5/24/2000 6.64 21.8 8.30 37.96 0.70791 JR-136 Water canal Nimrod 253.3 712.0 22.2 2/28/2001 5.96 18.9 7.28 1.70 JR-160 Water canal Nimrod 253.3 712.0 22.2 3/29/2001 5.16 20.8 7.51 2.45 JR-202 Water canal Nimrod 253.3 712.0 22.2 4/22/2001 5.66 19.9 7.17 2.94 JR-271 Water canal Nimrod 253.3 712.0 22.2 6/9/2001 5.43 25.7 7.41 0.90 JR-301 Water canal Nimrod 253.3 712.0 22.2 8/3/2001 5.35 24.0 7.25 1.13 JR-014 Wadi el maliach 251.4 696.1 38.1 9/11/1999 JR-12 Wadi el maliach 251.4 696.1 38.1 3/29/2000 6.20 20.4 8.00 JR-51 Wadi el maliach 251.4 696.1 38.1 5/23/2000 23.0 8.30 37.96 0.70776 JR-132 Wadi el maliach 251.4 696.1 38.1 2/27/2001 4.79 22.2 7.93 9.11 11 87 86 ID name E x N y Date Conductivity Temp pH D.O δ B Sr/ Sr Western inflows (Continued) m.s oC ‰ JR-235 Wadi el maliach 251.4 696.1 38.1 4/23/2001 4.87 24.4 7.87 9.58 JR-247 Wadi el maliach 251.4 696.1 38.1 6/4/2001 4.92 27.8 8.02 8.03 JR-369 Rafultzik-zarzir south 254.0 674.5 59.7 7/2/2002 80.60 36.9 7.50 JR-48 Tirtcha Upper 250.8 667.5 66.7 5/23/2000 25.9 8.50 40.21 0.70800 JR-129 Tirtcha Upper 250.8 667.5 66.7 2/27/2001 10.20 19.7 7.76 9.22 JR-243 Tirtcha Upper 250.8 667.5 66.7 6/4/2001 9.60 27.9 8.15 9.20 JR-7 Tirtcha Lower 252.0 661.5 72.7 3/29/2000 7.43 20.2 8.60 JR-127 Tirtcha Lower 252.0 661.5 72.7 2/27/2001 53.10 24.1 7.90 12.00 JR-6 Wadi el Ah'mar 249.1 659.2 75.0 3/29/2000 0.01 26.1 7.90 JR-46 Wadi el Ah'mar 249.1 659.2 75.0 5/25/2000 35.8 7.70 41.71 0.70796 JR-128 Wadi el Ah'mar 249.1 659.2 75.0 2/27/2001 83.90 24.5 7.50 5.80 JR-232 Wadi el Ah'mar 249.1 659.2 75.0 4/23/2001 77.70 27.6 7.64 7.50 JR-241 Wadi el Ah'mar 249.1 659.2 75.0 6/4/2001 100.00 38.5 8.03 7.30 JK-75 Wadi el Ah'mar 249.1 659.2 75.0 4/27/2005 79.00 22.1 7.38 JR-4 Uga Melecha 249.9 647.5 86.7 3/29/2000 8.44 19.7 8.10 JR-43 Uga Melecha 249.9 647.5 86.7 5/23/2000 22.0 8.50 41.71 0.70797 JR-77 Uga Melecha 249.9 647.5 86.7 8/7/2000 8.81 26.3 7.60 JR-229 Uga Melecha 249.9 647.5 86.7 4/23/2001 7.97 22.4 7.95 6.49 JR-333 Uga Melecha 249.9 647.5 86.7 8/3/2001 7.87 27.1 7.82 6.80 41.50 0.70804 JK-78 Uga village 4/26/2005 Springs and Groundwater JR-429 Shaar hagolan borehole 7/20/2003 JR-197 afikim - Groundwater 255.0 732.0 2.2 4/12/2001 22.73 0.70760 JR-356 afikim - Groundwater 254.5 731.5 2.7 1/3/2002 JR-424 Neve Ur- GW 6/12/2003 JR-19 Hamadia - Well 253.0 716.0 18.2 3/30/2000 6.11 22.9 7.30 JR-61 Hamadia - Well 253.0 716.0 18.2 5/24/2000 24.9 7.70 31.72 0.70741 JR-87 Hamadia - Well 253.0 716.0 18.2 8/8/2000 6.76 25.7 7.30 JR-167 Hamadia - Well 253.0 716.0 18.2 3/29/2001 6.57 24.5 7.35 3.73 JR-211 Hamadia - Well 253.0 716.0 18.2 4/22/2001 6.37 23.6 7.33 3.48 JR-265 Hamadia - Well 253.0 716.0 18.2 6/9/2001 6.14 25.0 7.15 8.20 JR-296 Hamadia - Well 253.0 716.0 18.2 8/3/2001 24.1 7.09 2.63 JR-73 En Huga (Soda Station) 250.6 713.9 20.4 5/24/2000 43.21 0.70783 11 87 86 ID name E x N y Date Conductivity Temp pH D.O δ B Sr/ Sr Springs and Groundwater (Continued) m.s oC ‰ JR-71 Hasida Spring 251.2 713.8 20.4 5/24/2000 23.3 8.00 43.71 JR-72 Hasida Spring Lower 251.2 713.3 20.9 5/24/2000 23.0 7.60 41.21 0.70780 JR-55 A-tin Spring 254.8 702.4 31.8 5/24/2000 6.10 22.0 8.40 34.22 0.70794 JR-13 Sukot Spring 251.7 696.8 37.4 3/29/2000 2.43 25.0 6.90 47.45 JR-52 Sukot Spring 251.7 696.8 37.4 5/23/2000 25.5 7.30 0.70798 JR-133 Sukot Spring 251.7 696.8 37.4 2/27/2001 2.38 24.8 6.73 5.95 JR-125 Tirtcha GW 251.7 696.8 70.6 2/27/2001 16.00 20.0 6.72 4.90 JR-101 Tirtcha Well 248.1 663.6 70.6 9/25/2000 38.10 27.7 6.60 JR-248 Uga Melecha-GW 249.9 647.5 86.7 6/9/2001 JR-1 Hagla - Well 248.3 637.5 96.7 3/29/2000 3.75 25.3 6.90 JR-41 Hagla - Well 248.3 637.5 96.7 5/23/2000 25.1 7.20 43.46 0.70799 JR-121 Hagla - Well 248.3 637.5 96.7 2/27/2001 4.01 24.5 6.75 3.60 JR-236 Hagla - Well 248.3 637.5 96.7 6/9/2001 3.90 25.0 7.00 2.90 Drainage JR-190 kav tet 2 253.5 733.4 0.8 4/12/2001 JR-194 afikim drainage 253.4 730.8 3.4 4/12/2001 JR-196 ashdot waste 254.2 729.3 4.9 4/12/2001 JR-191 Beit Zera - Cowshed 253.7 732.5 1.7 4/12/2001 JR-189 Degania b- kav tet 1 253.7 733.2 1.0 4/12/2001 26.47 0.70755 JR-192 Kelet -kav h 253.0 732.0 2.2 4/12/2001 JR-193 kochvani 253.0 731.5 2.7 4/12/2001 JR-277 Kochvani 253.0 731.5 2.7 8/3/2001 5.09 23.6 6.65 2.20 JR-354 Kochvani h1 253.0 732.0 2.2 1/3/2002 27.10 0.70754 JR-355 Kochvani h10 253.9 731.5 2.7 1/3/2002 JR-357 Kochvani Z 2 252.7 731.1 3.1 1/3/2002 JR-278 Robed 253.6 732.4 1.8 8/3/2001 2.40 24.5 7.39 5.19 JR-353 Robed gimel 1 253.6 732.4 1.8 1/3/2002 JR-352 Robed gimel 14 254.5 732.4 1.9 1/3/2002 JR-195 sephen ashdot 253.8 729.2 5.0 4/12/2001 JR-186 Sha'ar hagolan waste 257.5 731.1 3.1 4/12/2001 JR-184 Zor- Ashdot 256.1 728.8 5.4 4/12/2001 11 87 86 ID name E x N y Date Conductivity Temp pH D.O δ B Sr/ Sr Fish Pools m.s oC ‰ JR-95 Neve ur - pools 254.4 722.6 11.6 8/8/2000 9.55 32.4 8.20 JR-276 Neve ur - pools 254.4 722.6 11.6 8/3/2001 6.72 28.5 7.52 4.42 JR-166 Fish pond Hamadiya 252.3 715.0 19.2 3/29/2001 5.79 26.7 8.87 19.00 JR-208 Fish pond Hamadiya 252.3 715.0 19.2 4/22/2001 5.81 24.2 8.42 5.50 JR-266 Fish pond Hamadiya 252.3 715.0 19.2 6/9/2001 6.21 27.9 8.18 6.32 JR-86 Hamadia - Eden 251.0 713.5 20.7 8/8/2000 8.61 31.4 8.00 31.50 0.70762 JR-83 Tirat Zvi - pools 251.9 700.7 33.5 8/8/2000 6.67 30.4 7.70 JR-274 Hamadiya-zor 8/3/2001 7.57 28.8 7.53 3.81 JR-275 Hamadiya-H 8/3/2001 7.35 30.5 8.20 8.00 Western boreholes JR-510 Argaman swamp 63.0 6/24/2004 22.90 25.0 6.24 8.46 Jk-7 Borehole 1 11.0 10/15/2003 4.72 24.1 7.61 Jk-13 Borehole 1 11.0 3/9/2004 5.06 23.2 6.47 5.01 JK-61 Borehole 1 11.0 2/22/2005 4.11 23.5 6.25 6.14 Jk-6 Borehole 2 11.2 10/15/2003 6.80 23.9 7.80 Jk-12 Borehole 2 11.2 3/9/2004 9.20 24.0 6.50 1.80 Jk-30 Borehole 2 11.2 10/25/2004 7.27 24.9 6.50 2.13 JK-60 Borehole 2 11.2 2/22/2005 8.23 24.5 6.30 2.25 Jk-5 Borehole 3 13.2 10/15/2003 6.08 25.6 7.56 Jk-14 Borehole 3 13.2 3/9/2004 5.56 22.9 6.51 3.70 Jk-29 Borehole 3 13.2 10/25/2004 5.40 28.1 6.43 3.50 JK-55 Borehole 3 13.2 2/21/2005 5.34 22.7 6.49 4.50 Jk-3 Borehole 4 13.8 10/15/2003 19.40 26.5 7.56 Jk-10 Borehole 4 13.8 3/9/2004 21.20 25.6 6.57 2.75 Jk-27 Borehole 4 13.8 10/25/2004 19.20 27.1 6.87 1.59 JK-65 Borehole 4 13.8 2/22/2005 Jk-4 Borehole 5 13.8 10/15/2003 16.10 25.9 7.67 Jk-11 Borehole 5 13.8 3/9/2004 17.30 23.1 6.50 3.80 Jk-28 Borehole 5 13.8 10/25/2004 17.40 27.0 6.82 3.88 JK-66 Borehole 5 13.8 2/22/2005 Jk-2 Borehole 6 18.6 10/15/2003 16.30 25.4 7.51 Jk-8 Borehole 6 18.6 3/9/2004 15.80 22.6 6.18 0.29 Jk-31 Borehole 6 18.6 10/25/2004 14.20 25.5 6.32 1.20 11 87 86 ID name E x N y Date Conductivity Temp pH D.O δ B Sr/ Sr Western boreholes (Continued) m.s oC ‰ Jk-1 Borehole 7 18.6 10/15/2003 12.70 36.0 7.50 Jk-9 Borehole 7 18.6 3/9/2004 12.90 23.3 6.37 0.43 Jk-32 Borehole 7 18.6 10/26/2004 9.40 24.0 6.93 4.14 JK-57 Borehole 7 18.6 2/22/2005 9.40 22.0 6.64 4.36 JK-42 Borhole G-1 76.6 11/15/2004 43.00 26.0 5.80 2.00 JK-50 Borhole G-1 76.6 1/3/2005 34.40 24.2 7.21 3.99 JK-70 Borhole G-1 76.6 4/26/2005 31.00 26.0 6.50 JK-43 Borhole G-2 76.6 11/15/2004 82.00 26.0 6.10 0.60 JK-51 Borhole G-2 76.6 1/3/2005 90.90 24.2 7.44 2.03 JK-69 Borhole G-2 76.6 4/26/2005 84.00 26.0 6.40 JK-44 Borhole G-3 76.6 11/15/2004 JK-52 Borhole G-3 76.6 1/3/2005 >> 24.8 6.97 4.40 JK-68 Borhole G-3 76.6 4/26/2005 >> 28.0 6.00 JK-53 Borhole G-4 76.9 1/26/2005 >> 25.0 7.00 8.00 JK-67 Borhole G-4 76.9 4/26/2005 >> 25.0 6.10 JK-40 Borhole T-1 71.9 11/9/2004 87.70 26.1 6.30 0.83 JK-72 Borhole T-1 71.9 4/26/2005 81.00 28.0 6.30 JK-41 Borhole T-2 72.1 11/9/2004 73.70 25.5 7.31 0.40 JK-73 Borhole T-2 72.1 4/26/2005 75.00 27.0 6.20 JK-46 Borhole T-3 72.3 11/15/2004 >> 26.0 5.40 1.40 JK-71 Borhole T-3 72.3 4/26/2005 >> 27.0 6.10 JK-47 Borhole T-4 72.1 11/15/2004 58.00 25.0 5.70 2.00 JK-74 Borhole T-4 72.1 4/26/2005 28.00 25.0 6.60 Eastern inflows Yarmouk River 3535696 256.2 3240746 730.7 3.5 9/19/2000 888.00 28.5 7.00 C1 Igam well 3536390 262.6 3239859 723.4 10.8 6800 us/cm 23.5 7.60 11 Wadi Arab 3535145 255.3 3236050 722.0 12.2 9/19/2000 1091.00 40.4 6.97 25.72 0.70784 1A Wadi Arab 3535070 255.3 3235296 722.0 12.2 27/2/2001 2340.00 17.8 7.78 18.70 0.70775 1B Wadi Arab 3535070 255.3 3235296 722.0 12.2 4/9/2001 2440.00 20.3 8.16 Wadi Arab 3535070 255.3 3235296 722.0 12.2 8/21/2001 2020.00 26.0 7.52 JD1 Wadi Arab 255.3 3235296 722.0 12.2 12/1/2001 JF4 North Shuna thermal 12.0 2/1/2002 1113.00 49.8 7.08 JF5 North Shuna bridge 12.0 2/1/2002 11 87 86 ID name E x N y Date Conductivity Temp pH D.O δ B Sr/ Sr Eastern inflows (Continued) m.s oC ‰ JF6 Irbid westawater 2/1/2002 C5 Fish F. well 3534662 254.3 3235191 721.2 13.0 2740.00 21.8 7.48 2A Wadi Teibeh 3535530 256.0 3233830 717.7 16.5 2/27/2001 3360.00 20.1 8.00 2B Wadi Teibeh 3535530 256.0 3233830 717.7 16.5 4/9/2001 4710.00 20.4 8.01 21.00 0.70790 Wadi Teibeh 3535530 256.0 3233830 717.7 16.5 8/21/2001 5190.00 24.3 7.52 JD2 Wadi Teibeh 256.0 3233830 717.7 16.5 12/1/2001 3A Waqqas 3535330 255.7 3233195 716.6 17.6 2/27/2001 1740.00 21.3 8.89 29.80 0.70793 3B Waqqas 3535330 255.7 3233195 716.6 17.6 4/9/2001 1390.00 23.1 8.64 Waqqas 3535330 255.7 3233195 716.6 17.6 8/21/2001 1767.00 27.8 7.96 JF8 Waqqas well 3537294 3232091 714.5 19.7 1/2/2002 704.00 48.2 6.88 JF7 Manshiya thermal 3537243 3234017 715.0 19.2 2/1/2002 720.00 47.2 7.53 JD3 Ziglab-Waqqas 12/1/2001 Wadi Ziglab 3534256 254.0 3230760 712.3 21.9 9/19/2000 904.00 26.7 6.87 JF9 Abu Ziad well 3533802 3249762 738.0 2/1/2002 2230.00 48.6 6.41 4A Abu Ziad 3534833 255.0 3230044 710.8 23.4 2/27/2001 846.00 20.6 8.97 28.80 0.70870 Abu Thableh 3535020 255.2 3228130 707.4 26.8 9/19/2000 1920.00 36.2 5.90 5A Abu Thableh 3535003 255.2 3228733 707.4 26.8 2/27/2001 902.00 20.0 8.68 C7 Sp. unnamed 3535028 255.1 3227608 707.1 27.1 2890.00 21.0 6.87 Zoor Tbdulla 3534610 254.5 3227215 705.7 28.5 9/19/2000 5540.00 30.2 7.95 JF10 Abu thableh spring 3537191 3227896 705.7 28.5 2/1/2002 1978.00 36.5 6.64 6A Masharie 3535047 255.3 3226927 705.1 29.1 2/27/2001 1249.00 21.4 8.15 C8 Mfadi well 3534738 254.6 3225111 702.6 31.6 2200.00 21.7 7.04 C11 Mahrab Abu Ahm. 3534917 255.0 3224906 702.4 31.8 2440.00 22.0 7.30 C9 Juneidi Sp. 3534912 255.0 3224714 702.0 32.2 2400.00 21.7 7.64 C10 Zenati F. well 3534976 255.0 3224689 701.8 32.4 2050.00 21.7 7.54 C12 Sp. Unnamed 3533876 253.3 3224109 700.7 33.5 1580.00 23.2 7.30 C14 Bassat Sharhabil 3534566 254.4 3223734 700.1 34.1 1710.00 22.5 7.38 7A Yabis 3533928 253.6 3222951 697.8 36.4 2/27/2001 1223.00 18.2 7.62 4B Yabis 3533928 253.6 3222951 697.8 36.4 4/9/2001 1530.00 19.6 8.20 C13 Bassat Abu Habil 3534842 254.8 3222243 697.3 36.9 1740.00 24.4 7.78 C19 Qarn Sp. 3534750 254.6 3220992 695.0 39.2 1610.00 25.5 6.90 C20 Abu Namroud Sp. 3534428 254.3 3220956 695.0 39.2 1790.00 20.9 7.43 8A Kharoub 3533715 253.3 3219259 691.0 43.2 2/27/2001 2680.00 22.6 8.60 11 87 86 ID name E x N y Date Conductivity Temp pH D.O δ B Sr/ Sr Eastern inflows (Continued) m.s oC ‰ C15 Speera Sp. 3534411 254.3 3217782 689.0 45.2 2670.00 25.7 7.30 9A Bassat Abu Hamid 3534395 254.3 3217778 688.3 45.9 2/27/2001 2220.00 26.1 7.23 5B Bassat Abu Hamid 3534395 254.3 3217778 688.3 45.9 4/9/2001 2570.00 27.1 7.35 Bassat Abu Hamid 3534395 254.3 3217778 688.3 45.9 8/21/2001 2590.00 27.3 7.15 JD4 Bassat Abu Hamid 254.3 3217778 688.3 45.9 12/1/2001 10A Bassat Al Amira 3534244 254.1 3216810 686.5 47.7 2/27/2001 2530.00 24.3 8.13 C16 Kufranja Sp. 3534233 253.8 3216220 686.3 47.9 930.00 20.4 8.45 10 Rajib Seebiya 3534241 254.0 3216143 685.2 49.0 9/19/2000 3090.00 24.7 6.69 26.97 0.70804 11A Rajib Seediya 3534232 254.0 3216239 685.2 49.0 2/27/2001 1550.00 22.1 8.53 7B Rajib Seediya 3534232 254.0 3216239 685.2 49.0 4/9/2001 3370.00 26.1 8.07 Rajib Seediya 3534232 254.0 3216239 685.2 49.0 8/21/2001 3470.00 27.7 7.45 JD5 Rajib Seediya 254.0 3216239 685.2 49.0 12/1/2001 C17 Faleh Sp. 3534744 254.8 3214887 683.6 50.6 2780.00 23.8 8.15 8 Bassat Faleh 3534700 254.8 3214962 683.1 51.1 9/18/2000 2520.00 27.9 6.84 30.22 0.70806 12A Bassat Faleh 3534755 254.8 3214860 683.1 51.1 2/27/2001 2680.00 24.5 8.24 8B Bassat Faleh 3534755 254.8 3214860 683.1 51.1 4/9/2001 3200.00 27.3 8.17 Bassat Faleh 3534755 254.8 3214860 683.1 51.1 8/21/2001 3190.00 27.6 7.54 9 Bassat Faleh Wadi Botton 3534606 254.6 3214780 682.7 51.5 9/18/2000 4370.00 26.6 7.22 40.46 0.70809 JD6 Bassat Faleh 254.6 3214780 682.7 51.5 12/1/2001 C18 Buweib Sp. 3534407 254.3 3214111 682.3 51.9 1200.00 21.3 8.09 7 Bweib 3534398 254.3 3214092 681.5 52.7 9/18/2000 2690.00 26.4 6.79 29.22 0.70797 13A Bweib 3534403 254.3 3214118 681.5 52.7 2/27/2001 3060.00 23.7 8.35 9B Bweib 3534403 254.3 3214118 681.5 52.7 4/9/2001 3030.00 24.6 8.17 Bweib 3534403 254.3 3214118 681.5 52.7 8/21/2001 3590.00 27.1 7.60 JD7 Bweib 254.3 3214118 681.5 52.7 12/1/2001 El Kheil 3534587 3213077 54.0 8/21/2001 4870.00 26.9 7.75 C22 Kafir Sp. 3534604 254.5 3212957 680.2 54.0 4670.00 22.8 8.08 10B Kafir 3534543 3213074 680.0 54.2 4/9/2001 4050.00 25.1 8.33 JD8 Kafir 3213074 680.0 54.2 12/1/2001 C21 Sp. unnamed 3534563 254.4 3212725 679.8 54.4 5430.00 22.4 8.06 14A Mikman 3534561 254.6 3212735 679.0 55.2 2/27/2001 5000.00 23.6 8.30 11B Wadi Mikman 3534561 254.6 3212735 679.0 55.2 4/9/2001 6140.00 26.1 8.18 Wadi Mikman 3534561 254.6 3212735 679.0 55.2 8/21/2001 6120.00 27.2 7.87 11 87 86 ID name E x N y Date Conductivity Temp pH D.O δ B Sr/ Sr Eastern inflows (Continued) m.s oC ‰ 12 Wadi Mikman 3534572 254.6 3212735 678.9 55.3 9/18/2000 5640.00 26.2 6.79 26.22 0.70804 JD9 Mikman 254.6 3212735 678.9 55.3 12/1/2001 22A Twal (west) Hawaya 3534258 254.1 3211750 677.2 57.0 2/27/2001 4580.00 23.7 7.79 19B Twal (west) Hawaya 3534258 254.1 3211750 677.2 57.0 4/9/2001 5600.00 22.6 8.38 Twal (west) Hawaya dry 3534258 254.1 3211750 677.2 57.0 8/21/2001 13 Hawwaya 3534255 254.1 3211771 677.2 57.0 9/18/2000 6750.00 24.8 6.78 19.73 0.70820 JF12 Deir Alla thermal well 3538785 3211415 677.0 57.2 2/1/2002 11650.00 34.9 5.99 14 Mifshel 3533962 253.6 3210825 675.4 58.8 9/18/2000 7020.00 23.4 6.79 28.97 0.70827 21A Mifshel 3533985 253.6 3210828 675.4 58.8 2/27/2001 7040.00 19.8 8.21 21B Mifshel 3533985 253.6 3210828 675.4 58.8 4/9/2001 8370.00 21.9 8.24 Mifshel- dry 3533985 253.6 3210828 675.4 58.8 8/21/2001 20A Bassat Shakran 3533980 253.7 3210291 674.5 59.7 2/27/2001 2310.00 24.4 8.22 20B Bassat Shakran 3533980 253.7 3210291 674.5 59.7 4/9/2001 2660.00 25.2 7.91 JD18 Bassat Sakran 253.7 3210291 674.5 59.7 12/1/2001 6 Zarqa River 3533010 252.2 3206788 667.9 66.3 9/18/2000 6250.00 28.2 7.18 24.73 0.70871 18A Zarqa River 3532971 252.2 3206763 667.9 66.3 2/27/2001 5960.00 19.4 8.07 24.23 0.70868 17B Zarqa River 3532971 252.2 3206763 667.9 66.3 4/9/2001 7470.00 21.2 8.26 27.50 0.70857 Zarqa River 3532971 252.2 3206763 667.9 66.3 8/21/2001 7670.00 30.7 7.57 JD16 Zarqa 252.2 3206763 667.9 66.3 12/1/2001 4 Rasif 3533150 252.4 3205182 665.0 69.2 9/18/2000 20800.00 19.7 6.60 33.72 0.70836 17A Rasif 3533079 252.4 3205183 665.0 69.2 2/27/2001 14630.00 22.3 7.84 14B Rasif 3533079 252.4 3205183 665.0 69.2 4/9/2001 22400.00 21.6 8.10 Rasif 3533079 252.4 3205183 665.0 69.2 8/21/2001 25900.00 36.6 7.77 JD15 Rasif 252.4 3205183 665.0 69.2 12/1/2001 5 Abu Mayyala 3532642 251.6 3204603 663.9 70.3 9/18/2000 16300.00 18.9 6.32 28.72 0.70822 23A Abu Mayyala 3532657 251.6 3203752 663.9 70.3 2/27/2001 13400.00 20.2 8.09 15B Abu Mayyala-Mallaha 3532642 251.6 3204603 663.9 70.3 4/9/2001 18300.00 21.6 7.94 Abu Mayyala 3532642 251.6 3204603 663.9 70.3 8/21/2001 20600.00 32.1 7.55 JD14 Abu Mayalla 251.6 3204603 663.9 70.3 12/1/2001 Aqraa 3532393 251.2 3204603 663.9 70.3 9/18/2000 65500.00 21.3 6.69 24A Aqraa 3532163 251.2 3203426 663.9 70.3 2/27/2001 55900.00 23.7 7.69 48.20 0.70802 16B Aqraa 3532163 251.2 3203426 663.9 70.3 4/9/2001 89400.00 23.8 7.75 48.60 0.70794 Aqraa 3532163 251.2 3203426 663.9 70.3 8/21/2001 96700.00 36.3 7.18 11 87 86 ID name E x N y Date Conductivity Temp pH D.O δ B Sr/ Sr Eastern inflows (Continued) m.s oC ‰ JD13 Aqraa 251.2 3203426 663.9 70.3 12/1/2001 15 Mallah Gdeida 3533814 253.4 3204567 663.8 70.4 9/18/2000 5830.00 25.8 6.82 28.47 0.70807 19A Mallah Gdeida 3533865 253.4 3209358 663.8 70.4 2/27/2001 5020.00 24.3 7.33 18B Mallah Gdeida 3533865 253.4 3209358 663.8 70.4 4/9/2001 6430.00 24.7 7.49 Mallah Gdeida 3533865 253.4 3209358 663.8 70.4 8/21/2001 4960.00 26.6 6.96 JD17 Mallah Gdeida 253.4 3209358 663.8 70.4 12/1/2001 C23 Qurein pool 3533462 252.9 3203355 662.3 71.9 37300.00 30.2 7.59 25A Mallaha 3533774 253.4 3203311 661.7 72.5 2/27/2001 16040.00 25.7 8.33 29.47 0.70810 Mallaha 3533774 253.4 3203311 661.7 72.5 8/21/2001 3 Bassat El Faras 3534712 254.8 3159378 654.1 80.1 9/13/2000 31.22 0.70803 JD12 Bassat El Faras 254.8 3159378 654.1 80.1 12/1/2001 Wadi Mallaha Karama 3533410 252.8 3158840 653.3 80.9 9/13/2000 17810.00 32.4 7.22 JF15 Wadi Kafrain well 3540531 3150770 638.0 96.2 12/1/2001 653.00 16.2 8.03 JF14 Rama well 3540652 3150397 637.5 96.7 12/1/2001 5180.00 33.5 6.43 2 Kharar 3533586 253.2 3150282 637.4 96.8 9/13/2000 8050.00 24.8 7.08 28.97 0.70805 16A Kharar 3533539 253.2 3150282 637.4 96.8 2/27/2001 3790.00 24.2 7.64 13B Kharar 3533539 253.2 3150282 637.4 96.8 4/9/2001 5330.00 22.6 8.01 JD11 Kharar 253.2 3150282 637.4 96.8 12/1/2001 JF13 Hisban well 3541647 3149383 635.5 98.7 12/1/2001 6400.00 37.0 6.50 1 Hisban Kafrain 3533640 253.3 3149190 635.4 98.8 9/13/2000 8330.00 26.1 6.47 40.21 0.70816 15A Hisban Kafrain 3533530 253.3 3149159 635.4 98.8 2/27/2001 4760.00 18.7 7.92 12B Hisban Kafrain 253.3 3149159 635.4 98.8 4/9/2001 6940.00 19.3 7.93 JD10 Hisban 253.3 3149159 635.4 98.8 12/1/2001 JF3 Himma maqla spring 2/1/2002 1440.00 37.5 7.01 C2 Tell well 3450.00 19.9 7.45 C3 Waked well 1 3610.00 21.3 7.03 C4 Waked well 2 35800.00 21.6 8.56 34 18 ID name δ S δ O Ca Mg Na K Cl SO4 HCO3 NO3 Br B Sr PO4 TDS River ‰‰mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L JR-007 Alumot Bridge 19.6 424 120 1100 61 2426 172 344 1.0 25.00 0.60 8.7 4673 JR-26 Alumot Bridge -4.10 466 118 1111 54 2588 182 356 3.3 27.00 0.72 9.1 12.2 4905 JR-70 Alumot Bridge -4.40 418 113 1078 48 2445 185 339 3.8 41.00 0.62 8.7 6.4 4671 JR-92 Alumot Bridge 20.0 393 108 988 48 2213 171 312 1.0 30.00 0.49 7.8 4264 JR-106 Alumot Bridge -4.20 400 110 1015 48 2260 173 303 1.0 23.00 0.49 8.0 4332 JR-117 Alumot Bridge -4.40 409 109 992 53 2218 165 381 1.0 34.30 0.54 7.7 5.3 4362 JR-147 Alumot Bridge -4.30 347 98 850 49 1860 150 368 2.0 18.50 0.45 6.9 5.2 3742 JR-178 Alumot Bridge 359 97 855 48 1970 150 347 2.0 19.00 0.55 7.0 6.0 3846 JR-223 Alumot Bridge 378 105 930 48 2070 160 351 2.7 22.00 0.50 7.5 2.0 4067 JR-251 Alumot Bridge -4.05 363 104 950 42 2040 158 400 2.5 18.90 0.54 7.4 2.5 4079 JR-281 Alumot Bridge 427 109 960 54 2235 172 347 32.1 21.10 0.47 7.6 9.4 4357 JR-27 Beit Zera -3.80 371 104 897 46 2052 177 368 0.1 20.00 0.63 7.2 8.7 4035 JR-69 Beit Zera -4.30 410 114 1023 47 2478 193 329 4.0 23.00 0.58 8.3 3.0 4621 JR-93 Beit Zera 390 110 988 46 2229 182 310 4.5 22.00 0.49 7.8 4281 JR-108 Beit Zera -4.60 413 116 1040 42 2361 183 322 2.0 31.00 0.51 8.2 4510 JR-116 Beit Zera -4.50 356 102 865 42 1917 163 354 7.5 26.90 0.47 6.7 8.0 3833 JR-145 Beit Zera -5.00 388 109 940 45 2100 176 334 3.5 20.50 0.54 7.7 5.0 4116 JR-177 Beit Zera 414 109 945 47 2250 175 373 2.0 22.00 0.55 7.7 4.0 4337 JR-221 Beit Zera 378 108 925 42 2090 170 310 3.0 20.30 0.50 7.5 2.0 4046 JR-253 Beit Zera -3.75 346 95 810 41 1933 153 332 2.5 17.70 0.54 6.3 3.9 3730 JR-283 Beit Zera 368 103 875 42 2024 157 334 5.0 17.10 0.44 6.8 5.0 3925 JR-341 Beit Zera 388 114 955 47 2188 170 344 5.0 32.00 0.45 7.7 4243 JR-366 Beit Zera 327 99 850 48 1792 157 361 8.0 19.00 0.53 6.0 3.5 3661 JR-367 Beit-Zera Up 343 100 830 51 1820 162 373 8.0 17.00 0.52 6.3 3.5 3704 JR-365 Ubadia 310 100 850 43 1880 186 342 8.0 20.00 0.57 7.0 3.5 3739 JR-358 Menahamia 357 116 912 46 1953 195 354 6.0 19.00 0.67 6.7 3.5 3958 JR-006 Dalhamiya Bridge 9.6 374 138 1025 58 2295 284 325 3.6 22.30 0.80 7.5 4525 JR-23 Dalhamiya Bridge -3.60 357 126 920 48 1990 290 398 32.4 20.60 0.69 6.7 5.8 4181 JR-68 Dalhamiya Bridge -3.40 402 128 1022 50 2345 263 351 3.0 23.00 0.72 7.9 4.8 4588 JR-91 Dalhamiya Bridge 13.5 -4.20 355 110 885 46 2040 220 322 2.0 27.00 0.60 6.8 4007 JR-144 Dalhamiya Bridge -4.20 357 123 890 49 1983 250 388 4.0 26.20 0.73 8.1 4.7 4070 JR-176 Dalhamiya Bridge 366 115 850 45 1950 220 373 2.0 19.00 0.65 6.6 4.0 3940 JR-220 Dalhamiya Bridge 382 121 965 48 2140 230 351 2.0 21.30 0.65 7.4 2.5 4260 34 18 ID name δ S δ O Ca Mg Na K Cl SO4 HCO3 NO3 Br B Sr PO4 TDS River (Continued) ‰‰mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L JR-254 Dalhamiya Bridge -3.85 369 112 920 47 2100 198 342 2.5 19.90 0.62 6.9 3.5 4110 JR-304 Dalhamiya Bridge 372 117 950 48 2097 190 353 21.5 20.70 0.50 7.1 5.0 4169 JR-340 Dalhamiya Bridge 369 121 945 48 2170 200 351 5.0 33.00 0.50 7.4 4242 JR-360 Dalhamiya Bridge 345 124 928 47 1959 239 361 5.0 19.00 0.75 7.0 3.5 4027 JR-455 Dalhamiya Bridge 270 99 660 34 1586 225 98 30.0 12.50 5.2 3015 JR-24 Naharayim -4.90 349 129 908 47 1889 300 383 13.1 31.60 0.70 6.6 8.3 4050 JR-66 Naharayim -3.40 387 138 1005 48 2416 313 351 7.8 22.00 0.87 7.5 5.9 4689 JR-89 Gesher 11.7 -3.60 366 126 970 50 2300 270 327 7.0 28.00 0.70 7.3 4443 JR-114 Gesher -3.90 342 136 882 46 1888 327 378 18.0 27.00 0.77 6.0 7.9 4045 JR-142 Gesher -4.20 346 128 871 46 1941 275 355 10.7 25.70 0.81 7.8 5.4 3999 JR-174 Gesher 397 128 920 48 2160 270 354 7.0 20.00 0.70 7.1 6.0 4304 JR-218 Gesher 400 133 1020 50 2225 260 325 7.1 22.60 0.70 7.7 3.4 4442 JR-256 Gesher -3.02 390 124 935 51 2177 224 327 7.8 21.00 0.63 7.3 3.4 4257 JR-284 Gesher 395 124 960 47 2195 220 325 41.3 21.10 0.55 7.3 8.5 4328 JR-363 Gesher 320 130 910 48 1994 276 342 19.0 23.00 0.78 7.0 3.5 4062 JR-21 N.Ur north (78) -2.90 287 159 855 41 1708 464 390 21.2 17.30 0.75 5.4 9.7 3943 JR-64 N.Ur north (78) -2.80 338 153 983 46 2124 395 332 8.0 24.00 0.94 6.9 4403 JR-94 N.Ur north (78) 4.3 -2.70 338 167 980 48 2090 470 317 7.0 26.00 0.90 6.6 4443 JR-105 N.Ur north (78) -3.60 325 145 880 43 1905 365 342 11.8 24.50 0.85 6.6 2.0 4041 JR-112 N.Ur north (78) -3.40 320 160 887 45 1837 416 372 19.8 26.20 0.91 5.6 4.8 4083 JR-141 N.Ur north (78) -3.60 324 148 882 45 1890 372 354 13.5 22.20 0.83 7.4 5.1 4051 JR-171 N.Ur north (78) 356 154 920 46 2040 410 354 9.0 18.50 0.90 6.5 3.0 4307 JR-214 N.Ur north (78) 365 152 1000 48 2120 370 325 10.0 21.50 0.75 7.2 2.0 4411 JR-259 N.Ur north (78) -2.11 325 145 920 48 2056 317 317 7.8 19.70 0.77 6.6 2.5 4156 JR-288 N.Ur north (78) 380 152 1010 48 2240 300 312 12.8 21.60 0.64 7.2 5.0 4476 JR-364 N.Ur north (78) 290 155 890 43 1872 402 342 19.0 26.00 0.96 6.9 3.5 4039 JR-504 N.Ur north (78) 320 144 843 39 1917 380 342 21.7 16.40 0.83 6.0 1.0 4023 JR-464 N.Ur north (78) 177 93 465 21 940 290 332 25.0 7.90 3.1 2351 Jk-36 N.Ur north (78-pump) 300 148 890 45 1834 450 334 19.0 20.00 5.6 4040 Jk-37 N.Ur north (78-river) 295 145 890 44 1845 445 339 20.0 19.00 5.5 4042 JK-62 N.Ur north (78) 199 111 537 28 1076 310 334 24.0 8.00 3.5 2627 JR-22 N.Ur south (74) -3.10 273 155 765 38 1531 462 390 32.0 75.00 0.86 4.9 10.0 3721 JR-65 N.Ur south (74) -3.30 295 147 781 39 1630 490 368 18.0 18.00 0.88 5.4 3787 34 18 ID name δ S δ O Ca Mg Na K Cl SO4 HCO3 NO3 Br B Sr PO4 TDS River (Continued) ‰‰mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L JR-96 N.Ur south (74) 4.9 -3.30 297 145 790 42 1700 370 383 12.0 22.00 0.80 5.4 3760 JR-104 N.Ur south (74) -3.30 326 145 885 43 1910 360 339 9.3 19.30 0.85 6.6 2.0 4037 JR-113 N.Ur south (74) 292 151 791 42 1650 422 390 24.4 24.20 0.84 4.9 5.9 3787 JR-140 N.Ur south (74) -3.50 296 144 760 41 1599 380 375 19.6 18.40 0.85 6.3 6.0 3633 JR-170 N.Ur south (74) 316 146 815 41 1850 390 361 12.0 17.00 0.80 5.6 5.0 3948 JR-212 N.Ur south (74) 306 146 770 39 1635 370 366 14.0 15.90 0.70 5.3 2.0 3661 JR-261 N.Ur south (74) -1.90 288 149 860 44 1755 359 337 14.0 17.00 0.80 5.5 2.5 3823 JR-291 N.Ur south (74) 338 159 915 43 1965 330 325 14.8 18.20 0.64 6.1 5.0 4108 JR-503 N.Ur south (74) 276 146 716 35 1577 400 381 24.2 13.20 0.85 4.9 1.0 3568 JR-508 N.Ur south (74) JR-502 N.Ur south (74) 265 140 695 35 1527 400 376 25.2 12.70 0.84 4.7 1.0 3476 JR-463 N.Ur south (74) 179 97 455 22 890 315 339 25.0 7.00 3.0 2329 JK-63 N.Ur south (74) 182 104 488 26 974 295 347 23.0 8.70 3.1 2448 Jk-38 N.Ur south (74) 273 138 795 41 1624 420 361 19.0 16.00 4.9 3687 JR-462 Gimel 73 171 93 440 20 870 300 332 26.0 7.20 2.9 2259 JR-507 Gimel 73 Jk-35 Gimel 73 271 136 770 40 1570 410 358 23.0 17.00 4.8 3595 JK-64 Gimel 73 185 105 484 26 980 314 351 25.0 7.10 3.1 2478 JR-18 Hamadiya North (56) -3.30 266 162 737 39 1517 508 395 51.4 31.90 0.86 4.7 4.7 3707 JR-63 Hamadiya North (56) -3.10 271 157 770 39 1596 440 376 24.0 15.00 0.95 5.0 3687 JR-169 Hamadiya North (56) 300 175 850 44 1800 510 353 15.0 16.00 0.95 5.3 2.0 4063 JR-210 Hamadiya North (56) 299 166 812 44 1700 485 395 19.5 15.90 0.85 5.2 4.3 3937 JR-262 Hamadiya North (56) -1.83 276 158 870 45 1789 407 325 16.6 16.90 0.85 5.3 3.0 3903 JR-292 Hamadiya North (56) 289 157 817 39 1862 370 359 18.5 15.40 0.67 5.1 5.0 3927 JR-500 Hamadiya North (56) 275 155 735 35 1614 450 376 27.4 13.00 0.85 4.9 1.0 3680 JR-461 Hamadiya North (56) 179 118 470 22 900 400 349 26.0 7.20 3.0 2471 JR-505 Hamadiya North (56) Jk-34 Hamadiya North (56) 276 148 800 42 1630 455 358 23.0 17.00 5.0 3749 JK-59 Hamadiya North (56) 178 129 517 25 1050 350 376 13.0 7.40 3.1 2645 JR-509 Shaar 58 JR-501 Canal 56 gimel 253 168 755 36 1638 450 361 19.4 13.00 0.89 4.6 1.0 3693 JR-460 Canal 56 gimel 174 118 480 24 930 385 346 23.0 7.50 2.9 2488 JR-506 Canal 56 gimel 34 18 ID name δ S δ O Ca Mg Na K Cl SO4 HCO3 NO3 Br B Sr PO4 TDS River (Continued) ‰‰mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L Jk-33 Canal 56 gimel 244 152 805 40 1662 445 303 13.0 16.00 4.7 3680 JK-56 Canal 56 gimel 174 119 475 26 957 355 361 23.0 6.90 3.0 2497 JR-20 Hamadiya South (Zor) -5.10 263 162 745 42 1476 530 395 31.6 14.60 0.86 4.7 4.7 3660 JR-62 Hamadiya South (Zor) -2.70 267 157 771 39 1540 440 366 24.0 16.00 0.64 5.0 3621 JR-88 Hamadiya South (Zor) -3.10 273 151 765 41 1620 420 378 18.0 15.00 0.80 5.0 3681 JR-111 Hamadiya South (Zor) -3.30 275 166 755 40 1533 515 386 27.1 22.30 0.93 4.5 6.8 3719 JR-139 Hamadiya South (Zor) -3.30 270 160 729 39 1493 460 388 21.0 11.30 1.07 5.7 4.8 3571 JR-165 Hamadiya South (Zor) 295 166 785 40 1700 490 393 16.0 15.00 0.80 5.0 4.0 3900 JR-209 Hamadiya South (Zor) 300 166 814 44 1690 475 386 17.8 15.80 0.80 5.2 3.3 3908 JR-263 Hamadiya South (Zor) -1.94 274 161 865 44 1806 433 342 14.5 17.10 0.84 5.3 2.9 3956 JR-294 Hamadiya South (Zor) 300 164 814 40 1724 370 376 16.4 14.30 0.70 5.1 5.0 3819 JR-162 g-48 283 171 860 39 1780 425 383 9.0 13.00 0.70 4.8 4.0 3963 JR-204 g-48 273 172 825 49 1585 415 460 14.9 14.30 0.80 4.7 2.0 3808 JR-269 g-48 263 160 840 41 1764 400 354 11.8 15.50 0.78 4.6 2.5 3849 JR-298 g-48 271 170 910 38 1880 345 435 26.3 13.20 0.60 4.2 5.0 4089 JR-16 Maoz Haim -3.20 235 157 797 34 1534 445 412 14.9 12.50 0.72 3.8 7.7 3642 JR-57 Maoz Haim -3.10 241 164 850 36 1680 435 405 9.0 15.00 0.98 4.3 3835 JR-137 Maoz Haim -3.30 252 163 780 35 1624 405 425 13.2 16.00 0.80 4.8 4.0 3713 JR-161 Maoz Haim 259 161 828 36 1710 390 403 8.0 12.00 0.70 4.2 3.5 3807 JR-203 Maoz Haim 260 167 790 41 1520 405 478 11.5 13.50 0.80 4.5 2.0 3686 JR-270 Maoz Haim 262 160 840 40 1719 393 361 8.0 15.00 0.78 4.5 2.5 3798 JR-300 Maoz Haim 260 173 865 37 1851 360 401 6.0 13.90 0.60 4.0 5.0 3967 JR-013 Sheich Husein Bridge -1.08 225 174 850 41 1750 435 356 13.4 14.80 0.90 4.0 3859 JR-15 Sheich Husein Bridge -3.40 228 155 713 33 1385 431 415 27.3 21.20 0.70 3.8 4.1 3409 JR-53 Sheich Husein Bridge -2.50 234 164 844 34 1660 410 410 7.0 14.00 0.80 4.1 3776 JR-135 Sheich Husein Bridge -3.10 237 159 723 32 1490 375 405 12.4 15.00 0.75 4.5 2.7 3448 JR-159 Sheich Husein Bridge 265 166 810 35 1680 400 395 7.5 13.00 0.70 4.2 3.0 3772 JR-201 Sheich Husein Bridge 250 168 790 37 1630 410 403 10.5 13.20 0.75 4.3 2.5 3711 JR-272 Sheich Husein Bridge 243 160 845 39 1693 382 408 6.4 12.90 0.75 4.4 2.5 3789 JR-302 Sheich Husein Bridge 238 173 845 34 1758 330 390 27.1 11.90 0.57 3.8 5.0 3807 JR-339 Sheich Husein Bridge 259 188 840 37 1770 380 390 6.5 20.00 0.60 4.4 3891 JR-414 Sheich Husein Bridge 38 15 43 6 60 45 142 8.0 1.00 0.07 0.3 358 JR-422 Sheich Husein Bridge 95 61 217 11 415 171 239 23.0 3.00 1.0 1235 34 18 ID name δ S δ O Ca Mg Na K Cl SO4 HCO3 NO3 Br B Sr PO4 TDS River (Continued) ‰‰mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L JR-453 Sheich Husein Bridge 53 25 86 7 150 70 180 11.9 0.90 0.6 584 JR-004 Shifa' Station 3.8 195 182 770 34 1571 415 334 11.0 11.40 0.70 3.5 3523 JR-14 Shifa' Station -3.70 226 163 732 33 1300 397 427 28.9 10.40 0.62 3.8 1.8 3317 JR-54 Shifa' Station -2.80 219 168 825 33 1644 420 434 7.0 13.00 0.82 3.9 3763 JR-84 Shifa' Station 5.9 -2.40 250 170 810 36 1670 370 429 10.0 16.00 0.70 4.3 3761 JR-110 Shifa' Station -2.70 244 164 748 37 1551 444 377 21.3 21.30 0.84 4.0 4.9 3607 JR-134 Shifa' Station -3.10 235 167 747 33 1498 380 410 17.5 15.00 0.78 4.6 2.2 3503 JR-158 Shifa' Station 237 167 825 33 1660 375 410 13.0 12.00 0.65 4.1 2.0 3732 JR-200 Shifa' Station 240 178 820 35 1570 390 410 14.8 12.50 0.75 4.2 2.0 3670 JR-273 Shifa' Station 229 181 865 37 1702 390 403 5.6 12.40 0.70 4.2 2.5 3825 JR-303 Shifa' Station 205 187 880 37 1784 380 303 8.1 16.90 0.64 3.9 3801 JR-11 Gibton 212 158 624 28 1300 397 395 28.9 10.40 0.60 3.5 1.8 3154 JR-50 Gibton -3.30 136 173 657 26 1360 370 249 3.0 9.10 0.82 3.0 2983 JR-82 Gibton 1.9 -3.00 167 185 775 35 1570 410 259 5.0 13.00 0.90 3.5 3418 JR-157 Gibton 227 192 724 33 1510 440 412 14.0 11.00 0.75 3.8 2.0 3563 JR-246 Gibton 168 176 735 33 1600 415 212 4.0 10.90 0.62 3.4 3354 JR-81 Zarzir Station-58 6.3 -2.20 170 191 750 47 1470 520 288 11.0 12.00 1.00 4.0 3458 JR-103 Zarzir Station-58 -2.20 205 184 725 37 1475 440 364 18.3 10.80 0.80 4.0 0.1 3458 JR-131 Zarzir Station-58 -3.70 210 177 674 38 1331 440 405 31.4 12.80 0.84 4.9 1.2 3319 JR-156 Zarzir Station-58 217 209 765 39 1540 510 415 14.0 12.00 0.85 4.2 2.0 3720 JR-183 Zarzir Station-58 227 194 778 52 1530 475 412 19.5 12.50 0.95 4.0 2.0 3700 JR-234 Zarzir Station-58 250 232 865 58 1635 710 422 28.4 27.00 1.20 5.1 2.0 4228 JR-245 Zarzir Station-58 170 197 690 37 1460 475 290 6.5 9.10 0.63 3.6 3335 JR-337 Zarzir Station-58 -1.70 182 233 825 51 1658 650 264 6.0 19.00 0.90 4.1 3888 JR-370 Zarzir Station-58 195 208 825 44 1731 480 329 15.0 19.00 0.97 4.0 3846 JR-406 Zarzir Station-58 168 212 760 45 1623 525 256 5.0 11.00 0.90 4.0 3605 JR-421 Zarzir Station-58 120 62 225 18 455 195 244 20.0 4.00 1.0 1343 JR-428 Zarzir Station-58 233 223 815 38 1696 560 351 15.00 1.10 5.0 3931 JR-003 Adam Bridge 6.3 183 191 765 53 1450 611 303 29.9 9.90 1.10 4.6 3595 JR-010 Adam Bridge 5.6 -1.38 205 190 815 43 1680 517 327 23.0 13.70 0.90 4.2 1.2 3814 JR-9 Adam Bridge -3.40 234 193 758 44 1432 570 403 43.6 51.80 0.90 4.6 4.6 3729 JR-49 Adam Bridge -3.40 199 229 889 62 1480 715 322 22.0 12.00 1.40 5.7 3930 JR-80 Adam Bridge 7.2 -3.20 181 191 790 54 1500 590 285 14.0 11.00 1.10 4.5 3617 34 18 ID name δ S δ O Ca Mg Na K Cl SO4 HCO3 NO3 Br B Sr PO4 TDS River (Continued) ‰‰mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L JR-102 Adam Bridge -2.10 214 180 730 43 1460 500 351 20.6 10.50 0.85 4.5 0.1 3509 JR-130 Adam Bridge -3.10 222 182 694 43 1456 490 395 31.0 13.00 0.97 5.2 0.7 3526 JR-155 Adam Bridge -3.50 245 220 845 50 1670 630 390 17.0 13.00 1.05 4.9 2.0 4080 JR-233 Adam Bridge 280 265 1000 66 1915 795 420 24.4 16.90 1.40 6.0 2.0 4782 JR-244 Adam Bridge 173 190 720 46 1450 595 254 12.0 8.50 0.80 4.1 3448 JR-336 Adam Bridge -2.70 207 262 920 62 1893 730 244 13.0 23.00 1.10 5.2 4354 JR-371 Adam Bridge 216 224 930 60 1845 650 293 25.0 13.00 1.27 5.0 4256 JR-405 Adam Bridge 224 203 905 72 1788 770 300 12.0 12.00 1.30 5.0 4286 JR-410 Adam Bridge 208 117 522 35 1010 380 317 24.0 8.00 0.75 2.7 2621 JR-412 Adam Bridge 47 19 57 10 80 65 166 13.0 2.00 0.10 0.5 459 JR-420 Adam Bridge 113 72 244 15 480 204 256 20.0 4.00 2.0 1408 JR-452 Adam Bridge 68 39 137 11 262 115 202 16.0 1.80 1.0 852 JR-8 Tovlan Station -83 -3.40 244 200 808 49 1575 670 390 45.3 60.00 1.03 4.9 2.7 4042 JR-47 Tovlan Station -83 -3.20 252 286 1150 79 2258 1025 281 26.0 21.00 2.00 6.9 5377 JR-79 Tovlan Station -83 7.2 -2.10 209 229 975 69 1850 765 268 18.0 15.00 1.60 5.3 4398 JR-100 Tovlan Station -83 -1.70 232 200 810 50 1621 565 334 22.6 11.95 1.20 4.9 0.1 3846 JR-126 Tovlan Station -83 -3.70 243 203 806 51 1528 620 400 35.0 16.00 1.14 6.0 1.0 3902 JR-154 Tovlan Station -83 -3.40 286 253 990 61 1900 780 395 22.0 15.00 1.40 5.7 2.0 4702 JR-231 Tovlan Station -83 -3.10 335 315 1250 78 2525 1005 408 25.7 29.20 1.90 7.0 3.0 5970 JR-242 Tovlan Station -83 195 221 870 58 1670 720 246 14.4 11.10 1.00 4.7 4005 JR-335 Tovlan Station -83 -2.50 246 288 1175 86 2385 952 261 30.0 18.00 1.60 6.0 5441 JR-375 Tovlan Station -83 227 232 983 64 1950 750 254 10.0 14.00 1.52 5.0 4484 JR-404 Tovlan Station -83 273 246 1150 92 2151 970 18.0 17.00 2.11 6.0 4917 JR-413 Tovlan Station -83 53 23 80 13 125 80 178 12.0 2.00 0.13 0.5 566 JR-427 Tovlan Station -83 290 297 1100 53 2250 750 368 21.00 1.50 6.7 5129 JK-48 Tovlan Station -83 228 195 867 45 1795 479 353 12.00 0.90 3.0 3974 JK-55 Tovlan Station -83 -3.50 252 179 765 52 1480 640 454 46.0 9.00 1.20 5.0 3877 JK-77 Tovlan Station -83 290 257 1020 66 2044 880 398 36.0 15.30 1.70 6.0 5006 JR-5 Gilgal - 107 -3.40 251 205 825 50 1606 667 395 46.2 25.00 1.05 5.0 4071 JR-45 Gilgal - 107 -2.80 258 299 1175 75 2309 968 278 23.0 21.00 1.90 6.9 5406 JR-78 Gilgal - 107 7.1 -1.90 207 226 935 64 1870 740 268 19.0 20.00 1.50 5.2 4350 JR-153 Gilgal - 107 -3.40 260 250 1000 61 1910 780 386 32.0 10.00 1.30 5.7 2.0 4688 JR-230 Gilgal - 107 -3.40 345 335 1290 78 2660 980 383 24.6 24.60 1.85 7.2 3.0 6120 34 18 ID name δ S δ O Ca Mg Na K Cl SO4 HCO3 NO3 Br B Sr PO4 TDS River (Continued) ‰‰mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L JR-240 Gilgal - 107 178 200 805 54 1550 660 255 14.2 10.00 1.25 4.3 3726 JR-334 Gilgal - 107 -2.10 244 327 1250 91 2485 980 215 32.0 34.00 1.70 6.2 5658 JR-403 Gilgal - 107 277 282 1205 89 2400 975 256 18.0 27.00 1.70 7.0 5529 JK-45 Gilgal - 107 230 196 865 45 1785 486 354 13.00 1.10 5.0 3974 JK-54 Gilgal - 107 -3.70 254 181 775 54 1526 670 154 50.0 10.00 1.30 5.0 3674 JK-76 Gilgal - 107 300 273 1101 70 2178 890 398 37.0 17.50 6.60 7.0 5265 JR-44 Zur el mandase -3.30 282 319 1243 81 2453 1010 293 26.0 25.00 2.10 7.9 5732 JR-002 Alenby Bridge 5.8 225 257 1060 79 2040 902 244 30.0 14.80 1.90 6.2 4851 JR-011 Alenby Bridge 5.0-5.6 -2.02 237 207 880 56 1862 695 359 34.0 16.80 1.35 4.9 4346 JR-3 Alenby Bridge -3.40 257 218 860 54 1655 745 386 40.3 16.50 1.25 5.3 3.1 4232 JR-42 Alenby Bridge -3.30 281 319 1233 81 2380 1030 300 26.0 22.00 1.75 7.8 5673 JR-76 Alenby Bridge 5.0 -2.40 226 252 1120 76 1980 780 250 17.0 23.00 1.80 4724 JR-97 Alenby Bridge -2.20 250 217 895 57 1807 640 327 22.7 13.30 1.40 5.5 0.1 4229 JR-124 Alenby Bridge -3.50 256 218 856 56 1735 690 390 36.5 17.00 1.50 6.6 1.0 4255 JR-152 Alenby Bridge -3.40 385 358 1340 80 2710 1090 403 27.0 25.00 1.85 8.2 5.0 6418 JR-228 Alenby Bridge -3.20 325 300 1185 78 2430 950 366 27.4 21.10 1.90 7.1 3.0 5683 JR-239 Alenby Bridge 305 341 1365 95 2590 1100 264 27.5 21.20 2.15 7.8 6108 JR-332 Alenby Bridge -2.90 370 430 1700 134 3466 1460 237 25.0 45.00 2.50 9.5 7866 JR-372 Alenby Bridge 249 271 1150 79 2264 850 242 10.0 17.00 1.98 6.0 5132 JR-402 Alenby Bridge 306 320 1375 103 2818 1100 237 14.0 24.00 2.20 7.0 6297 JR-409 Alenby Bridge 235 147 645 38 1320 425 312 49.0 11.50 0.90 3.3 3183 JR-419 Alenby Bridge 95 61 211 14 415 175 227 15.0 3.00 1.0 1216 JR-451 Alenby Bridge 74 38 140 14 246 135 205 14.8 1.60 1.0 868 JR-001 Baptism site 5.7 225 261 1050 79 2086 898 242 29.6 16.10 1.80 6.4 4886 JR-012 Baptism site 5.6 -1.59 235 216 935 58 1880 563 351 25.4 13.00 1.30 5.0 1.7 4276 JR-2 Baptism site -4.10 269 227 897 57 1740 777 393 43.2 22.50 1.25 5.8 4425 JR-75 Baptism site 6.4 -4.70 238 275 1100 83 2200 870 251 17.0 29.00 1.90 6.5 5063 JR-98 Baptism site -1.40 250 219 895 58 1812 640 325 23.6 23.60 1.40 5.6 0.1 4245 JR-122 Baptism site -3.60 268 222 858 56 1759 680 386 36.7 19.60 1.47 6.9 1.0 4285 JR-151 Baptism site -3.30 381 255 1290 775 2660 1005 408 27.0 24.00 1.70 8.2 5.0 6825 JR-227 Baptism site -3.30 335 318 1230 80 2575 930 361 27.9 23.30 1.85 7.7 3.0 5880 JR-238 Baptism site 330 370 1450 103 2720 1160 259 21.2 21.90 2.20 8.7 6435 JR-331 Baptism site -2.30 500 592 2250 164 4672 1760 244 30.0 66.00 2.90 13.4 10278 34 18 ID name δ S δ O Ca Mg Na K Cl SO4 HCO3 NO3 Br B Sr PO4 TDS River (Continued) ‰‰mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L JR-373 Baptism site 268 292 1200 83 2443 870 259 19.0 35.00 2.01 6.6 5469 JR-401 Baptism site 341 366 1500 110 3103 1150 263 14.0 25.00 2.30 9.0 6872 JR-408 Baptism site 420 190 940 61 2030 820 241 53.0 18.00 1.25 4.8 4773 JR-411 Baptism site 92 52 211 17 410 170 222 20.0 3.00 0.30 1.2 1197 JR-418 Baptism site 96 62 214 15 420 179 222 15.0 3.00 1.0 1226 JR-426 Baptism site 388 428 1500 71 3300 910 376 35.00 2.00 9.7 7008 JR-99 Ab'dala Bridge -1.60 260 233 935 61 1927 650 320 23.5 20.20 1.40 5.9 0.1 4429 JR-123 Ab'dala Bridge -3.80 266 224 879 57 1780 690 390 37.0 18.00 1.47 7.0 1.0 4341 JR-150 Ab'dala Bridge -3.50 353 331 1220 79 2550 895 405 27.0 26.50 1.65 8.0 5.0 5887 JR-226 Ab'dala Bridge -3.30 325 317 1200 79 2490 890 376 28.3 22.70 1.80 7.6 3.0 5728 JR-237 Ab'dala Bridge 367 428 1662 109 3440 1270 271 23.6 26.90 2.40 9.8 7597 JR-330 Ab'dala Bridge -2.40 545 705 2300 170 5370 1650 254 20.0 81.00 2.80 13.9 11095 JR-374 Ab'dala Bridge 279 309 1250 88 2550 900 251 23.0 20.00 2.06 7.0 5670 JR-400 Ab'dala Bridge 336 376 1475 112 3260 1100 239 11.0 28.00 2.30 9.0 6937 JR-407 Ab'dala Bridge 334 192 900 51 1940 625 334 47.0 16.00 1.20 4.4 4439 JR-417 Ab'dala Bridge 96 61 208 14 415 175 222 15.0 3.00 1.0 1209 JR-425 Ab'dala Bridge 403 468 1550 77 3580 920 371 40.00 2.00 10.1 7409 Western inflows JR-118 Bitaniya 101 54 271 98 430 99 625 1.0 2.40 0.32 0.9 41.0 1681 JR-148 Bitaniya 102 53 263 97 442 96 683 1.9 2.50 0.20 0.9 48.0 1741 JR-180 Bitaniya 105 54 264 92 442 95 683 1.0 2.50 0.30 1.0 40.0 1739 JR-225 Bitaniya 4.60 58 91 275 90 474 88 732 1.0 2.40 0.30 0.9 37.0 1811 JR-249 Bitaniya 4.20 JR-280 Bitaniya 92 52 280 99 467 85 610 29.2 2.40 0.25 1.0 1.0 1717 JR-342 Bitaniya JR-351 Bitaniya JR-107 Saline carrier -4.40 398 103 935 42 2165 165 300 6.2 29.00 0.64 8.2 3.3 4144 JR-119 Saline carrier -4.70 494 126 1185 55 2775 184 349 3.4 44.40 0.60 9.4 4.3 5216 JR-149 Saline carrier -5.00 510 127 1175 53 2765 180 325 2.0 36.40 0.69 11.9 2.8 5173 JR-179 Saline carrier 386 104 940 42 2210 165 317 2.0 20.00 0.55 7.6 7.0 4186 JR-224 Saline carrier 434 114 1060 46 2395 173 295 5.6 24.00 0.55 8.8 2.0 4547 JR-250 Saline carrier -4.96 380 108 945 42 2070 158 322 25.0 19.80 0.50 7.6 3.5 4070 JR-279 Saline carrier 465 117 1080 47 2464 170 300 9.0 22.50 0.50 8.7 5.0 4674 34 18 ID name δ S δ O Ca Mg Na K Cl SO4 HCO3 NO3 Br B Sr PO4 TDS Western inflows (Continued) ‰‰mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L JR-343 Saline carrier 395 112 980 45 2256 160 312 5.0 32.00 0.45 8.0 4297 JR-350 Saline carrier 356 102 940 43 2003 146 23.00 0.60 7.1 3613 JR-146 W. Yavneal -3.70 75 50 148 4 247 95 266 42.5 0.60 0.19 1.2 1.0 928 JR-181 W. Yavneal 76 49 147 5 245 95 266 44.0 0.90 0.20 0.9 0.2 928 JR-222 W. Yavneal 75 50 150 3 235 97 268 45.0 1.00 0.15 1.0 1.0 924 JR-252 W. Yavneal -3.82 74 49 142 4 233 100 266 42.6 1.00 0.17 0.9 2.5 911 JR-282 W. Yavneal 72 48 145 4 211 97 264 39.9 1.00 0.15 0.9 1.0 881 JR-188 point 110 38 78 585 42 650 290 664 2.0 5.70 2.00 0.6 2.0 2354 JR-187 point 121 82 36 97 7 145 92 307 11.7 1.00 0.15 1.2 1.0 779 JR-344 point 121 77 37 101 9 145 0.15 1.4 369 JR-368 point 121 10.6 76 33 90 7 122 76 322 10.0 1.00 0.13 1.0 0.0 736 JR-185 Yarmuhim Reseruoir 82 37 100 7 150 94 312 9.5 1.00 0.15 1.2 1.0 793 JR-359 Yarmuhim Reseruoir 10.2 76 34 94 7 135 80 298 9.0 1.00 0.17 1.0 733 JR-005 Yarmuok River - Naharayim -2.1 146 198 630 31 1041 723 451 16.0 8.50 1.90 2.1 3245 JR-25 Yarmuok River - Naharayim -3.50 146 154 506 23 843 583 476 8.1 8.10 1.35 1.8 4.6 2746 JR-67 Yarmuok River - Naharayim -3.30 145 206 702 27 1130 710 432 10.0 10.00 2.22 2.1 3371 JR-90 Yarmuok River - Naharayim -2.70 158 232 715 32 1210 850 439 8.0 11.00 2.10 2.1 3655 JR-115 Yarmuok River - Naharayim -3.50 170 177 568 25 940 590 512 28.5 12.10 1.45 1.9 1.3 3023 JR-143 Yarmuok River - Naharayim 151 161 499 21 823 515 444 20.9 9.00 1.61 2.2 1.0 2644 JR-175 Yarmuok River - Naharayim 195 253 725 29 1330 853 442 15.0 11.00 2.20 2.3 2.0 3853 JR-198 Yarmuok River - Naharayim 204 298 825 30 1430 1020 469 14.5 13.00 2.50 2.6 2.0 4303 JR-219 Yarmuok River - Naharayim 162 238 720 28 1240 815 425 15.1 11.00 2.20 2.2 2.0 3654 JR-255 Yarmuok River - Naharayim -2.62 210 322 845 34 1546 1083 451 15.7 13.00 2.50 2.6 2.0 4520 JR-285 Yarmuok River - Naharayim 373 722 1550 51 3083 2390 398 22.3 26.90 5.00 3.7 5.0 8616 JR-361 Yarmuok River - Naharayim 181 203 637 27 1100 680 512 27.0 10.00 2.02 2.1 2.0 3377 JR-415 Yarmuok River - Naharayim 37 14 36 5 50 40 144 0.20 0.08 0.3 326 JR-423 Yarmuok River - Naharayim 61 35 99 8 155 105 227 20.0 1.00 1.0 711 JR-454 Yarmuok River - Naharayim 36 15 40 4 52 40 151 10.0 0.20 0.3 348 JR-173 Gesher drainage (81) 341 121 840 47 1940 260 315 7.0 18.00 0.70 7.4 2.0 3888 JR-217 Gesher drainage (81) 270 195 940 43 1890 520 288 5.7 18.50 1.00 6.1 2.0 4170 JR-257 Gesher drainage (81) 207 175 850 46 1700 502 271 2.9 16.30 1.37 4.8 2.5 3770 JR-286 Gesher drainage (81) 382 170 1280 71 2883 246 124 44.0 27.00 0.66 9.3 5.0 5227 JR-172 N.Ur - Water canal (78) 268 287 1090 47 1905 1250 347 8.0 15.00 1.70 5.2 2.0 5216 34 18 ID name δ S δ O Ca Mg Na K Cl SO4 HCO3 NO3 Br B Sr PO4 TDS Western inflows (Continued) ‰‰mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L JR-215 N.Ur - Water canal (78) 260 263 1100 47 1910 1050 327 7.5 17.00 1.50 5.5 2.0 4982 JR-258 N.Ur - Water canal (78) 285 186 1030 48 2221 405 273 2.9 20.70 1.00 6.6 2.5 4472 JR-287 N.Ur - Water canal (78) 323 217 1120 45 2560 422 305 36.0 22.80 0.92 7.0 16.2 5051 JR-213 N.Ur - Water canal (76) 320 178 1050 46 2155 460 288 2.0 4.40 0.85 6.2 2.0 4503 JR-260 N.Ur - Water canal (76) -0.69 300 170 1065 48 2233 396 239 2.5 22.40 0.90 6.1 2.5 4476 JR-290 N.Ur - Water canal (74) 308 173 985 51 2113 380 234 10.1 20.60 0.75 6.1 5.0 4274 JR-168 Hamadiya - south canal 259 195 855 40 1830 530 325 2.0 16.00 0.85 4.6 2.0 4052 JR-207 Hamadiya - south canal 218 173 825 40 1657 470 305 2.5 14.40 0.85 4.2 2.0 3705 JR-264 Hamadiya - south canal -0.96 259 190 920 45 1870 537 325 3.3 17.10 0.93 5.0 2.5 4166 JR-295 Hamadiya - south canal 286 227 955 45 2120 545 359 11.3 16.00 0.92 5.0 5.0 4564 JR-17 W. Harod -2.60 190 142 811 24 1728 193 398 1.5 7.60 0.50 2.3 5.4 3494 JR-60 W. Harod -2.90 216 148 905 28 1959 203 444 2.0 8.00 0.44 2.4 4.3 3914 JR-85 W. Harod 223 152 948 31 1865 200 459 1.0 8.30 0.39 2.4 3887 JR-138 W. Harod 207 144 792 25 1545 193 399 6.9 6.20 0.46 2.9 2.4 3318 JR-164 W. Harod 212 139 825 26 1750 180 395 3.0 7.00 0.35 2.3 2.0 3537 JR-206 W. Harod 209 145 795 30 1700 185 405 5.6 7.80 0.40 2.4 2.0 3482 JR-267 W. Harod 206 146 760 28 1578 203 410 9.4 7.70 0.42 2.3 2.7 3348 JR-297 W. Harod 214 142 830 30 1636 180 468 5.0 7.20 0.34 2.2 5.0 3512 JR-59 Water canal 48 -4.60 287 247 1099 27 2425 330 425 7.0 17.00 0.50 4.9 4864 JR-163 Water canal 48 250 200 900 23 2040 280 351 7.0 10.50 0.35 3.5 2.0 4062 JR-205 Water canal 48 280 226 1080 28 2362 325 437 7.2 13.50 0.45 4.5 2.0 4758 JR-268 Water canal 48 -0.76 236 184 890 31 1860 335 339 11.0 12.90 0.56 3.9 2.5 3899 JR-16 Water canal Nimrod -3.20 241 164 850 36 1680 435 405 9.0 15.00 0.70 4.3 3835 JR-58 Water canal Nimrod -3.80 256 237 804 18 1929 240 368 38.0 13.00 0.30 3.8 3903 JR-136 Water canal Nimrod -3.10 215 185 698 30 1506 270 549 2.0 13.50 0.55 3.9 1.8 3468 JR-160 Water canal Nimrod 212 168 642 28 1400 250 517 0.5 9.50 0.45 3.0 1.9 3227 JR-202 Water canal Nimrod 217 185 730 29 1510 310 490 3.1 15.80 0.60 3.4 2.0 3490 JR-271 Water canal Nimrod 208 185 740 34 1486 295 549 2.5 9.50 0.60 3.2 2.5 3509 JR-301 Water canal Nimrod 220 188 720 28 1506 290 512 17.8 10.60 0.47 3.2 5.0 3492 JR-014 Wadi el maliach 22.2 -4.11 255 108 675 42 1500 335 182 7.5 18.50 0.70 5.7 3123 JR-12 Wadi el maliach -4.30 229 105 552 29 1333 362 293 22.3 21.70 0.64 4.5 2945 JR-51 Wadi el maliach -4.60 250 117 632 35 1336 340 288 20.0 15.00 0.88 5.2 3033 JR-132 Wadi el maliach -4.20 235 105 632 36 1332 295 207 11.0 17.40 0.76 6.2 1.0 2871 34 18 ID name δ S δ O Ca Mg Na K Cl SO4 HCO3 NO3 Br B Sr PO4 TDS Western inflows (Continued) ‰‰mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L JR-235 Wadi el maliach 240 118 614 35 1291 354 281 20.4 14.80 0.75 4.8 2968 JR-247 Wadi el maliach 277 128 665 38 1398 360 303 17.4 13.00 0.61 5.3 3199 JR-369 Rafultzik-zarzir south 2090 3610 15800 930 36140 4200 168 170.0 635.00 25.13 56.0 63743 JR-48 Tirtcha Upper -4.30 339 474 1257 88 2677 1340 1171 16.0 24.00 2.35 9.3 7386 JR-129 Tirtcha Upper -4.80 330 473 1315 97 2536 1480 554 30.0 35.00 2.64 11.0 1.0 6850 JR-243 Tirtcha Upper 290 445 1200 100 2460 1570 523 19.6 20.20 2.10 7.8 6628 JR-7 Tirtcha Lower 0.10 232 281 1033 98 2188 870 276 0.1 21.00 2.20 5.3 6.5 4999 JR-127 Tirtcha Lower -1.10 1620 2545 9050 856 22503 3830 200 10.0 360.00 11.40 52.0 10.0 40974 JR-6 Wadi el Ah'mar -0.90 3650 3885 14050 1010 37990 1770 129 24.9 782.00 3.65 65.5 63291 JR-46 Wadi el Ah'mar 4.3 -3.00 3530 3976 13820 1133 37900 1810 112 0.1 630.00 4.65 69.5 62911 JR-128 Wadi el Ah'mar 3580 4060 14700 1110 39630 1730 122 10.0 580.00 12.61 80.0 10.0 65522 JR-232 Wadi el Ah'mar -1.40 3200 3465 13100 980 36700 1800 159 20.0 575.00 3.80 61.0 30.0 59999 JR-241 Wadi el Ah'mar 4870 5250 18800 1415 52896 2550 98 110.0 660.00 6.70 86649 JK-75 Wadi el Ah'mar 3500 3605 12954 905 36356 1950 117 20.0 468.00 12.00 66.0 59875 JR-4 Uga Melecha -5.20 338 369 1120 103 2547 1023 347 36.4 33.30 2.20 6.4 5916 JR-43 Uga Melecha -4.70 301 329 984 91 2250 930 327 31.0 31.00 2.50 5.8 5274 JR-77 Uga Melecha -17.1 -6.20 301 343 1025 100 2250 890 310 30.0 30.50 2.60 5.8 5278 JR-229 Uga Melecha -5.30 290 335 1010 96 2354 940 312 38.0 30.00 2.40 5.6 5406 JR-333 Uga Melecha -16.7 305 350 1000 100 2338 920 317 25.0 36.00 2.00 5.7 5391 JK-78 Uga village 53 26 22 3 42 18 236 17.2 0.24 0.03 0.1 417 Springs and Groundwater JR-429 Shaar hagolan borehole 118 151 400 33 553 620 512 2.5 4.00 1.10 2.0 1.0 2394 JR-197 afikim - Groundwater 179 196 575 64 820 885 442 82.0 8.20 1.80 2.1 2.0 3251 JR-356 afikim - Groundwater 188 182 590 54 1045 681 488 52.0 10.00 1.82 2.0 2.0 3290 JR-424 Neve Ur- GW 495 1100 3100 130 3490 6600 586 20.00 6.30 9.7 15521 JR-19 Hamadia - Well -2.40 230 203 805 32 1589 623 388 8.1 100.00 0.78 4.2 1.8 3978 JR-61 Hamadia - Well -1.40 199 195 763 31 1500 550 395 0.5 16.00 0.87 3.7 3650 JR-87 Hamadia - Well -0.90 236 219 825 36 1690 560 417 1.0 15.00 1.00 4.3 3999 JR-167 Hamadia - Well 258 222 870 36 1890 540 408 2.0 17.00 0.90 4.4 2.0 4242 JR-211 Hamadia - Well 250 219 872 36 1810 545 400 2.0 17.00 0.90 4.4 2.0 4151 JR-265 Hamadia - Well -1.82 235 203 860 36 1745 509 381 3.4 16.40 0.89 4.3 2.5 3988 JR-296 Hamadia - Well 257 232 870 36 1847 500 386 25.7 14.50 0.80 4.4 5.0 4169 JR-73 En Huga (Soda Station) -3.00 246 151 662 18 1560 230 344 22.0 9.00 0.34 2.8 3241 34 18 ID name δ S δ O Ca Mg Na K Cl SO4 HCO3 NO3 Br B Sr PO4 TDS Springs and Groundwater (Con) ‰‰mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L JR-71 Hasida Spring -3.30 239 158 721 24 1629 260 344 32.0 10.00 0.38 2.8 3417 JR-72 Hasida Spring Lower -3.30 253 167 682 26 1635 210 342 23.0 11.00 0.35 2.7 3349 JR-55 A-tin Spring -1.80 221 270 747 18 1888 270 415 3.0 14.00 0.53 4.8 3845 JR-13 Sukot Spring -4.80 147 90 230 4 445 178 451 100.4 2.90 0.27 1.2 1648 JR-52 Sukot Spring -4.80 146 87 240 4 430 170 451 100.0 3.00 0.34 1.2 1632 JR-133 Sukot Spring -4.80 145 85 220 5 395 163 459 94.0 1.90 0.33 1.3 1.0 1568 JR-125 Tirtcha GW -4.90 823 609 1960 214 5180 1640 276 3.0 68.00 3.64 26.5 3.0 10773 JR-101 Tirtcha Well -2.40 660 1080 6100 530 14124 645 322 40.0 192.00 10.00 13.0 0.1 23693 JR-248 Uga Melecha-GW 44 16 69 12 104 110 82 0.1 0.43 0.20 0.5 0.1 436 JR-1 Hagla - Well -5.50 238 171 252 47 890 328 268 40.0 4.90 0.55 9.2 2239 JR-41 Hagla - Well -5.00 238 175 287 49 950 340 249 41.0 5.00 0.68 9.6 2333 JR-121 Hagla - Well -5.70 255 180 269 48 990 350 261 41.5 9.60 0.72 11.7 1.0 2404 JR-236 Hagla - Well 246 179 284 50 950 373 261 39.6 4.40 0.65 9.8 2386 Drainage JR-190 kav tet 2 2.00 JR-194 afikim drainage 175 158 615 42 990 613 525 2.0 9.20 1.60 2.2 2.0 3129 JR-196 ashdot waste 98 49 300 95 460 38 820 1.0 2.30 0.25 0.9 46.5 1863 JR-191 Beit Zera - Cowshed JR-189 Degania b- kav tet 1 363 206 620 55 1150 1010 486 128.0 10.20 1.60 2.3 2.0 4027 JR-192 Kelet -kav h JR-193 kochvani 216 176 655 44 1130 750 473 5.6 10.30 1.70 2.7 2.0 3460 JR-277 Kochvani 222 185 700 48 1150 756 471 5.1 10.50 1.80 2.7 2.0 3548 JR-354 Kochvani h1 93 68 328 35 645 166 293 1.0 3.00 0.36 1.1 5.0 1632 JR-355 Kochvani h10 70 52 280 36 450 160 307 1.0 3.00 0.31 1.0 6.0 1359 JR-357 Kochvani Z 2 235 165 700 48 1194 782 449 2.0 11.00 1.69 2.8 2.0 3586 JR-278 Robed 89 85 275 32 370 332 371 50.0 2.50 0.67 1.2 1606 JR-353 Robed gimel 1 JR-352 Robed gimel 14 139 152 466 53 644 710 459 90.0 5.00 1.68 2.0 1.0 2718 JR-195 sephen ashdot 80 48 274 24 480 3 542 1.0 4.30 0.20 1.0 18.0 1456 JR-186 Sha'ar hagolan waste JR-184 Zor- Ashdot 57 88 680 59 735 412 708 42.0 6.40 4.50 1.0 1.0 2787 34 18 ID name δ S δ O Ca Mg Na K Cl SO4 HCO3 NO3 Br B Sr PO4 TDS Fish Pools ‰‰mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L JR-95 Neve ur - pools -0.80 303 168 1100 56 2500 386 153 10.0 29.00 0.90 7.1 4705 JR-276 Neve ur - pools 250 187 995 49 2150 452 129 5.0 19.70 0.85 5.4 5.0 4237 JR-166 Fish pond Hamadiya 237 164 765 42 1630 506 217 2.0 15.00 0.85 4.5 2.0 3578 JR-208 Fish pond Hamadiya 212 160 806 45 1605 500 244 2.0 14.80 0.90 4.4 2.0 3589 JR-266 Fish pond Hamadiya -0.19 228 179 890 50 1807 548 178 2.5 17.40 0.98 4.8 2.5 3900 JR-86 Hamadia - Eden 0.40 266 201 980 54 2030 610 261 10.0 24.00 1.20 5.6 4436 JR-83 Tirat Zvi - pools 2.90 153 186 707 26 1770 220 84 10.0 15.00 0.40 2.5 3171 JR-274 Hamadiya-zor 262 230 1130 64 2350 640 188 15.7 22.30 1.20 6.1 5.0 4901 JR-275 Hamadiya-H 335 164 1110 53 2460 348 144 34.4 23.70 0.70 7.2 5.0 4672 Western boreholes JR-510 Argaman swamp 675 870 3050 260 6665 2500 378 80.00 24.0 14478 Jk-7 Borehole 1 134 154 620 11 880 700 327 29.6 5.50 1.07 3.7 2861 Jk-13 Borehole 1 163 142 660 8 870 780 427 71.0 4.90 4.8 3126 JK-61 Borehole 1 117 121 585 7 800 495 440 52.0 4.00 4.0 2621 Jk-6 Borehole 2 129 202 975 10 1610 700 407 15.1 14.00 1.45 4.2 4062 Jk-12 Borehole 2 298 325 1135 12 1930 1350 456 170.0 15.00 7.4 5691 Jk-30 Borehole 2 192 240 1100 14 1840 900 376 8.0 17.00 5.7 4687 JK-60 Borehole 2 234 313 1230 15 2123 1100 403 44.0 15.00 7.5 5477 Jk-5 Borehole 3 182 182 781 39 1543 500 337 41.3 13.00 1.25 3.4 3618 Jk-14 Borehole 3 158 145 670 28 1325 375 346 22.0 11.00 2.7 3080 Jk-29 Borehole 3 160 144 700 40 1304 410 341 62.0 12.00 3.0 3173 JK-55 Borehole 3 -3.50 167 155 687 39 1380 298 25.0 9.80 3.0 2761 Jk-3 Borehole 4 345 595 2620 80 6132 400 298 17.6 72.00 2.00 9.1 10560 Jk-10 Borehole 4 347 630 2700 90 6330 400 288 2.9 75.00 9.8 10863 Jk-27 Borehole 4 303 557 2700 95 6020 360 300 10.0 71.00 8.7 10416 JK-65 Borehole 4 281 527 2450 90 5622 318 293 3.0 63.00 7.8 9647 Jk-4 Borehole 5 321 530 2130 62 4670 700 320 54.5 53.00 2.20 7.8 8841 Jk-11 Borehole 5 465 585 1950 50 5040 700 251 26.0 54.00 8.6 9121 Jk-28 Borehole 5 304 526 2350 75 5230 600 341 2.0 64.00 7.9 9492 JK-66 Borehole 5 286 517 2350 73 5252 535 312 4.0 56.00 7.9 9385 Jk-2 Borehole 6 608 595 1880 31 4286 1650 509 21.2 29.00 2.20 9.3 9609 Jk-8 Borehole 6 505 560 1810 41 3980 1600 495 1.0 25.00 9.5 9017 Jk-31 Borehole 6 400 510 1850 50 3737 1500 580 0.2 28.00 7.8 8655 34 18 ID name δ S δ O Ca Mg Na K Cl SO4 HCO3 NO3 Br B Sr PO4 TDS Western boreholes (Continued) ‰‰mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L Jk-1 Borehole 7 398 489 1390 43 3410 970 522 1.5 28.00 1.30 6.9 7252 Jk-9 Borehole 7 385 445 1425 43 3310 950 488 6.9 25.00 7.0 7078 Jk-32 Borehole 7 260 305 1230 41 2363 750 561 3.0 20.00 4.5 5533 JK-57 Borehole 7 275 330 1245 42 2540 685 549 2.0 17.00 5.0 5685 JK-42 Borhole G-1 1450 1900 5500 150 15260 1700 454 182.00 5.70 31.0 26596 JK-50 Borhole G-1 -2.80 1100 1450 4200 100 11925 1600 359 5.0 135.00 2.70 27.0 20874 JK-70 Borhole G-1 1150 1483 4212 100 11404 1700 561 10.0 120.00 3.00 25.0 20740 JK-43 Borhole G-2 3000 3900 11850 500 35000 1600 166 472.00 7.00 75.0 56488 JK-51 Borhole G-2 -1.95 3200 4550 14000 600 39718 1700 339 10.0 568.00 6.20 93.0 64685 JK-69 Borhole G-2 3315 4326 13770 555 39335 1900 137 20.0 513.00 7.00 87.0 63871 JK-44 Borhole G-3 5000 6300 19500 900 56626 2000 429 708.00 13.50 124.0 91463 JK-52 Borhole G-3 16.9 1.80 4200 5700 18500 920 53584 2000 159 50.0 758.00 9.50 125.0 85871 JK-68 Borhole G-3 3980 5428 17340 835 48546 2100 415 20.0 592.00 11.50 105.0 79256 JK-53 Borhole G-4 0.50 4850 7550 20200 945 61020 2500 400 144.0 777.00 10.90 105.0 98386 JK-67 Borhole G-4 4750 7673 21267 960 62763 2400 166 20.0 830.00 11.00 105.0 100829 JK-40 Borhole T-1 2700 4400 13700 600 37500 3150 325 440.00 10.00 62.0 62815 JK-72 Borhole T-1 2600 4326 13770 560 36391 2900 342 20.0 460.00 9.50 60.0 61369 JK-41 Borhole T-2 2850 3750 11250 420 31750 3050 154 387.00 11.00 55.0 53611 JK-73 Borhole T-2 2570 4120 11781 435 33400 3250 390 20.0 418.00 7.50 57.0 56384 JK-46 Borhole T-3 4600 7000 15700 565 52150 2050 342 702.00 14.00 98.0 83109 JK-71 Borhole T-3 4260 6746 15300 505 50047 2000 439 20.0 660.00 6.00 95.0 79977 JK-47 Borhole T-4 1850 2750 7660 180 22490 1800 359 269.00 3.70 52.0 37358 JK-74 Borhole T-4 860 1195 3978 110 10035 1400 461 10.0 116.00 3.00 24.0 18165 Eastern inflows 0 Yarmouk River 62 35 119 8 138 108 298 4.3 771 C1 Igam well 165 345 680 40 2060 230 212 25.00 0.80 2.3 3757 11 Wadi Arab 62 35 97 6 174 101 195 6.8 0.62 0.22 0.9 678 1A Wadi Arab -3.9 134 93 262 45 300 510 254.0 1.00 1.2 35.0 1599 1B Wadi Arab 121 58 223 49 312 246 586 108.0 2.05 0.57 0.7 30.0 1704 Wadi Arab 113 66 200 31 274 211 436 76.3 34.4 1408 JD1 Wadi Arab 113 50 164 31 230 207 317 110.0 0.50 0.57 0.7 12.0 1223 JF4 North Shuna thermal 84 45 87 5 118 86 385 2.0 1.00 0.16 1.0 2.0 813 JF5 North Shuna bridge 105 47 118 6 184 218 310 5.0 1.00 0.21 1.0 5.0 994 34 18 ID name δ S δ O Ca Mg Na K Cl SO4 HCO3 NO3 Br B Sr PO4 TDS Eastern inflows (Continued) ‰‰mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L JF6 Irbid westawater 100 37 188 43 254 108 610 5.0 4.00 0.63 1.0 35.0 1349 C5 Fish F. well 327 125 1120 22 2305 290 395 23.00 0.70 10.5 4607 2A Wadi Teibeh 244 220 412 47 515 1330 71.0 2.80 1.52 8.4 1.0 2842 2B Wadi Teibeh -5.4 306 242 423 56 553 1580 378 42.0 2.60 1.30 9.3 1.0 3583 Wadi Teibeh 340 303 400 39 757 1432 390 39.1 31.8 3699 JD2 Wadi Teibeh 271 219 411 49 520 1400 332 46.0 3.00 1.50 8.0 1.0 3251 3A Waqqas 72 115 199 8 245 400 34.0 1.10 0.52 2.4 1.0 1074 3B Waqqas 67 65 130 6 192 160 250 13.0 1.18 0.20 1.6 0.5 885 Waqqas 73 91 160 6 227 223 390 17.4 19.2 1187 JF8 Waqqas well 68 33 29 3 41 28 353 1.0 0.20 0.08 0.7 1.0 556 JF7 Manshiya thermal 75 36 24 2 37 42 367 1.0 0.10 0.06 0.4 1.0 583 JD3 Ziglab-Waqqas 84 51 51 5 119 69 342 16.0 0.40 0.07 0.7 1.0 737 Wadi Ziglab 62 34 71 6 108 77 248 42.2 648 JF9 Abu Ziad well 173 59 220 26 340 264 532 1.0 1.20 0.44 2.9 1.0 1616 4A Abu Ziad 56 47 74 7 118 99 4.5 0.40 0.14 0.9 1.0 406 Abu Thableh 144 57 204 18 331 159 435 31.0 1379 5A Abu Thableh 62 35 105 8 148 88 3.3 0.70 0.15 1.0 1.0 449 C7 Sp. unnamed 191 99 203 10 600 165 354 4.00 0.25 2.7 1626 Zoor Tbdulla 240 147 788 18 1513 468 361 40.3 3575 JF10 Abu thableh spring 153 49 188 15 314 178 485 1.0 1.40 0.33 2.3 1.0 1384 6A Masharie 119 59 114 7 194 145 16.0 0.80 0.16 1.0 1.0 654 C8 Mfadi well 79 65 87 5 225 87 273 1.30 0.18 2.3 822 C11 Mahrab Abu Ahm. 85 60 92 6 236 110 233 1.00 0.20 2.6 823 C9 Juneidi Sp. 79 65 133 8 272 120 263 2.00 0.33 3.0 942 C10 Zenati F. well 67 65 136 7 243 97 299 2.00 0.33 3.0 916 C12 Sp. Unnamed 80 40 77 4 137 83 288 0.80 0.20 1.0 710 C14 Bassat Sharhabil 99 52 94 6 200 117 271 1.00 0.17 1.0 840 7A Yabis 94 63 113 13 217 92 37.0 1.50 0.21 1.0 1.0 630 4B Yabis 68 67 125 16 231 98 342 30.0 1.72 0.20 1.0 0.5 978 C13 Bassat Abu Habil 63 53 87 4 180 68 248 1.00 0.30 0.9 704 C19 Qarn Sp. 93 72 105 7 260 45 371 1.30 0.25 1.1 954 C20 Abu Namroud Sp. 54 39 66 7 164 28 205 1.00 0.23 0.8 564 8A Kharoub 87 102 432 29 745 260 38.0 6.70 1.18 3.0 1.0 1699 34 18 ID name δ S δ O Ca Mg Na K Cl SO4 HCO3 NO3 Br B Sr PO4 TDS Eastern inflows (Continued) ‰‰mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L C15 Speera Sp. 106 52 132 12 236 223 237 1.80 0.38 2.5 1000 9A Bassat Abu Hamid 159 99 248 26 417 373 71.0 3.10 0.62 3.3 1.0 1395 5B Bassat Abu Hamid 116 101 247 27 420 365 360 61.0 3.06 0.50 3.1 1.0 1700 Bassat Abu Hamid 143 85 229 20 407 295 390 34.7 9.1 1602 JD4 Bassat Abu Hamid 130 93 237 24 422 350 307 65.0 3.00 0.60 3.0 1.0 1631 10A Bassat Al Amira 123 137 303 32 505 480 94.0 5.00 0.81 3.3 1.0 1678 C16 Kufranja Sp. 54 25 44 5 100 33 181 1.00 0.10 0.5 443 10 Rajib Seebiya 127 123 306 24 596 298 309 71.9 8.14 1.29 7.0 1862 11A Rajib Seediya 111 66 154 15 370 70 56.0 4.20 0.21 1.4 1.0 846 7B Rajib Seediya 128 122 332 30 806 119 317 67.0 9.90 0.34 2.5 1.0 1931 Rajib Seediya 149 106 400 23 881 72 344 72.5 11.6 2048 JD5 Rajib Seediya 162 102 261 23 687 108 356 69.0 8.00 0.33 2.0 1.0 1776 C17 Faleh Sp. 81 124 290 22 450 255 422 5.00 0.85 3.0 1649 8 Bassat Faleh 123 120 290 23 369 444 370 141.4 4.31 0.83 2.5 1883 12A Bassat Faleh 107 128 360 36 715 219 98.0 7.70 0.81 2.1 1.0 1670 8B Bassat Faleh 91 131 357 38 675 210 336 92.0 7.43 0.61 2.1 1.0 1937 Bassat Faleh 108 146 300 27 691 133 390 103.5 13.5 1898 9 Bassat Faleh Wadi Botton 251 184 457 40 1085 495 406 43.4 21.31 0.77 2.4 2982 JD6 Bassat Faleh 104 124 327 33 687 222 354 97.0 8.00 0.76 2.0 1.0 1956 C18 Buweib Sp. 37 42 80 9 142 85 166 1.00 0.20 0.7 562 7 Bweib 162 124 290 27 369 600 284 101.7 5.14 0.76 2.2 1962 13A Bweib 115 169 437 46 800 390 61.0 7.50 1.01 3.0 1.0 2025 9B Bweib 100 137 300 32 529 320 415 89.0 4.38 0.60 2.5 1.0 1926 Bweib 316 70 360 35 710 477 528 72.5 13.9 2568 JD7 Bweib 117 131 269 27 525 317 405 100.0 5.00 0.67 2.0 1.0 1896 El Kheil 116 221 600 62 852 858 448 102.9 22.7 3260 C22 Kafir Sp. 132 197 500 60 730 760 344 5.00 1.20 6.9 2728 10B Kafir 116 186 470 64 675 595 433 140.0 4.62 0.89 6.5 1.0 2684 JD8 Kafir 142 193 492 54 792 693 449 155.0 6.00 1.10 5.0 1.0 2976 C21 Sp. unnamed 144 161 515 58 650 905 249 4.00 1.20 8.0 2686 14A Mikman 248 281 790 108 1045 1560 158.0 4.80 2.05 12.1 1.0 4195 11B Wadi Mikman 224 273 757 115 973 1420 372 150.0 4.76 1.50 11.0 2.0 4289 Wadi Mikman 224 307 600 77 1003 1369 425 142.0 36.2 4147 34 18 ID name δ S δ O Ca Mg Na K Cl SO4 HCO3 NO3 Br B Sr PO4 TDS Eastern inflows (Continued) ‰‰mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L 12 Wadi Mikman 289 254 547 60 823 1344 375 151.3 5.09 1.81 9.8 3847 JD9 Mikman 220 252 735 98 1020 1430 410 152.0 5.00 1.90 10.0 2.0 4322 22A Twal (west) Hawaya 286 180 700 115 855 1415 111.0 2.60 2.65 14.5 1.0 3665 19B Twal (west) Hawaya 143 201 780 87 1070 1090 375 15.0 3.63 1.16 5.9 2.0 3765 Twal (west) Hawaya dry 0 13 Hawwaya 617 361 586 160 1053 2578 431 111.0 3.03 2.65 14.1 5900 JF12 Deir Alla thermal well 676 139 1890 148 2934 1460 1239 5.0 8.00 3.00 11.0 5.0 8499 14 Mifshel 349 337 697 170 996 2141 223 124.0 1.91 0.83 1.6 5038 21A Mifshel 280 280 1300 180 1630 2080 153.0 5.50 2.71 15.9 5.0 5909 21B Mifshel 262 273 1200 184 1515 2000 259 140.0 5.47 2.46 14.5 3.0 5838 Mifshel- dry 0 20A Bassat Shakran 90 88 345 39 470 320 0.7 1.90 0.82 1.8 1.0 1355 20B Bassat Shakran 72 83 318 41 460 320 426 2.3 1.85 0.60 1.7 1.0 1724 JD18 Bassat Sakran 174 196 740 74 1060 1100 433 10.0 4.00 1.40 5.0 2.0 3791 6 Zarqa River 353 219 708 65 1358 1118 351 62.6 10.44 2.27 7.7 4245 18A Zarqa River 9.5 240 210 1050 100 1710 1150 49.0 9.30 2.54 8.2 1.0 4518 17B Zarqa River 10.0 254 206 1070 106 1720 1140 290 1.0 9.02 2.07 8.4 3.0 4796 Zarqa River 301 151 933 92 1723 777 321 57.0 6.7 4355 JD16 Zarqa 300 212 1145 99 1968 1220 320 57.0 18.00 1.20 8.0 5339 4 Rasif 453 748 2729 134 4836 3038 312 112.2 87.71 8.09 12.8 12450 17A Rasif 705 680 3300 250 6025 3090 78.0 52.00 8.82 16.5 10.0 14180 14B Rasif 682 709 3553 283 6360 3220 279 94.0 87.00 7.00 16.3 10.0 15267 Rasif 1430 516 3500 269 7904 2028 229 88.7 41.0 15965 JD15 Rasif 782 666 3220 249 6322 3020 337 66.0 43.00 7.60 16.0 10.0 14705 5 Abu Mayyala 327 308 3150 152 4357 2496 390 126.5 53.91 7.47 14.9 11360 23A Abu Mayyala 750 640 2850 224 5220 3030 150.0 46.00 8.54 15.7 10.0 12910 15B Abu Mayyala-Mallaha 708 576 2800 246 4835 3010 279 140.0 41.10 6.30 15.7 10.0 12635 Abu Mayyala 747 774 3000 269 5822 3213 218 161.8 29.9 14205 JD14 Abu Mayalla 794 649 2930 237 5470 2980 237 135.0 44.00 8.00 16.0 10.0 13476 Aqraa 940 4605 11035 802 30525 2328 740 232.5 51207 24A Aqraa 2370 4590 16700 1055 41500 4190 84.0 545.00 20.63 45.2 50.0 71034 16B Aqraa 10.2 1970 4500 17000 1150 38230 4140 267 500.0 740.00 20.72 43.0 50.0 68497 Aqraa 2571 4933 15999 847 39852 4236 218 262.9 36.1 68918 34 18 ID name δ S δ O Ca Mg Na K Cl SO4 HCO3 NO3 Br B Sr PO4 TDS Eastern inflows (Continued) ‰‰mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L mg/L JD13 Aqraa 2020 4160 15500 985 38000 4100 293 50.0 470.00 8.40 37.0 50.0 65578 15 Mallah Gdeida 309 249 506 102 964 1296 371 5.6 7.84 11.56 14.1 3811 19A Mallah Gdeida 320 230 300 95 1100 1550 57.0 4.00 2.30 1.8 1.0 3656 18B Mallah Gdeida 264 236 865 101 1150 1530 449 47.0 4.08 1.63 6.4 3.0 4646 Mallah Gdeida 449 100 600 46 928 1025 528 35.3 19.5 3711 JD17 Mallah Gdeida 295 210 724 73 1070 1300 430 45.0 4.00 0.80 5.0 2.0 4151 C23 Qurein pool 1100 1415 6450 380 12220 4800 220 125.00 20.50 26.0 26710 25A Mallaha 5.6 740 608 3850 306 5900 3930 138.0 36.00 13.26 15.0 10.0 15508 Mallaha 0 3 Bassat El Faras 21.88 7.12 13.3 22 JD12 Bassat El Faras 760 443 2215 130 3670 3230 239 112.0 16.00 6.00 14.0 10.0 10815 Wadi Mallaha Karama 820 568 3209 127 5786 2933 188 144.5 13775 JF15 Wadi Kafrain well 71 20 35 5 69 67 210 1.0 0.30 0.07 0.4 1.0 478 JF14 Rama well 249 90 730 94 1146 343 956 6.0 3.00 1.10 6.0 2.5 3617 2 Kharar 453 224 1117 132 2205 888 689 13.6 18.40 1.59 20.7 5741 16A Kharar 170 148 600 43 1240 330 5.9 8.00 0.80 26.0 1.0 2544 13B Kharar 197 172 635 46 1335 378 352 4.6 8.33 0.97 27.0 2.0 3128 JD11 Kharar 758 610 1770 118 4629 1650 400 28.0 35.00 2.20 36.0 10.0 9998 JF13 Hisban well 340 108 900 113 1556 500 955 2.5 5.00 1.40 5.0 2.5 4480 1 Hisban Kafrain 471 237 1090 155 2336 830 610 61.4 25.74 0.82 9.9 5817 15A Hisban Kafrain 366 285 755 41 2245 450 69.0 20.00 0.64 6.8 1.0 4231 12B Hisban Kafrain 350 283 725 57 2005 494 176 83.0 18.50 0.68 6.6 2.0 4192 JD10 Hisban 229 135 334 25 937 285 273 41.0 8.00 0.37 3.0 2.0 2267 JF3 Himma maqla spring 124 33 120 14 195 160 337 1.0 2.00 0.18 3.0 5.0 986 C2 Tell well 110 93 422 25 660 310 476 5.00 0.45 2.2 2101 C3 Waked well 1 180 120 388 15 740 440 378 5.00 0.65 2.1 2266 C4 Waked well 2 1235 256 5600 55 13400 200 51 145.00 2.80 57.0 20942