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: dee concentrations and 6° crprc value versus the FIG. 37. Diagram of the HCO; and CO, concentrations and 6" crpic value versus the individual sampling events of the water of the Kuzuluk Mineral Spring.

Figure 37 : dee concentrations and 6° crprc value versus the FIG. 37. Diagram of the HCO; and CO, concentrations and 6" crpic value versus the individual sampling events of the water of the Kuzuluk Mineral Spring.

Related Figures (41)

FIG. 1. Investigation area of the Maramara Project [2].
FIG. 1. Investigation area of the Maramara Project [2].
FIG. 2. Tectonic Map of Western Turkey including active fault zones and epicenters of former strong earthquakes (MTA).
FIG. 2. Tectonic Map of Western Turkey including active fault zones and epicenters of former strong earthquakes (MTA).
FIG. 3. Tectonic Sketch Map of Western Turkey with active fault zones and epicenter of the Izmit,17 August 1999 earthquake [5].
FIG. 3. Tectonic Sketch Map of Western Turkey with active fault zones and epicenter of the Izmit,17 August 1999 earthquake [5].
FIG. 4. Diagram of the measured wate temperature and electrical conductivity of the Armutlu. Borehole outflow at the instance: between July 1992 and July 2001 (red star i: indicating the occurence of the Izmit 17.8.199' Earthquake).
FIG. 4. Diagram of the measured wate temperature and electrical conductivity of the Armutlu. Borehole outflow at the instance: between July 1992 and July 2001 (red star i: indicating the occurence of the Izmit 17.8.199' Earthquake).
FIG. 6. Diagram of the Na and K concentration of the Yalova thermal spring at the instances between July 1992 and July 2001 (red star-> occurrence of the Izmit 17.8.1999 Earthquake).
FIG. 6. Diagram of the Na and K concentration of the Yalova thermal spring at the instances between July 1992 and July 2001 (red star-> occurrence of the Izmit 17.8.1999 Earthquake).
As process which has induced the observed variations of NO3, F, Ca and Cl concentrations most probably is the intrusion of shallow groundwater of the Gemlik plain which contains also some amounts of pollutants, as indicated by the increase of the NO; concentration. FIG. 8. Diagram of the K, NO; and F concentration of the water of the Gemlik Kaplica at the instances between July 1992 and July 2001.
As process which has induced the observed variations of NO3, F, Ca and Cl concentrations most probably is the intrusion of shallow groundwater of the Gemlik plain which contains also some amounts of pollutants, as indicated by the increase of the NO; concentration. FIG. 8. Diagram of the K, NO; and F concentration of the water of the Gemlik Kaplica at the instances between July 1992 and July 2001.
FIG. 10. Diagram of the Li, NH, and Br concentration of the Kuzuluk thermal water at the instances between July 1988 and July 2001.
FIG. 10. Diagram of the Li, NH, and Br concentration of the Kuzuluk thermal water at the instances between July 1988 and July 2001.
FIG. 9. Diagram of the Na, Ca, Mg, SO, and Cl concentration of the water of the Gemlik Kaplica at the instances between July 1992 and July 2001 (red star > occurrence of the Izmit 17.8.1999 Earthquake).
FIG. 9. Diagram of the Na, Ca, Mg, SO, and Cl concentration of the water of the Gemlik Kaplica at the instances between July 1992 and July 2001 (red star > occurrence of the Izmit 17.8.1999 Earthquake).
FIG. 11. Diagram of the Na and Cl concentration of the Kuzuluk thermal water at the instances between July 1988 and July 2001 (red star-> occurrence of the Izmit 17.8.1999 Earthquake).
FIG. 11. Diagram of the Na and Cl concentration of the Kuzuluk thermal water at the instances between July 1988 and July 2001 (red star-> occurrence of the Izmit 17.8.1999 Earthquake).
The most probable explanations are also related to mixing processes including 1) components a of dee seated fluids, ii) the thermal water itself and iii) a shallow component of oxygenated water injected i the deep aquifer which would also react with therein contained uranium minerals.
The most probable explanations are also related to mixing processes including 1) components a of dee seated fluids, ii) the thermal water itself and iii) a shallow component of oxygenated water injected i the deep aquifer which would also react with therein contained uranium minerals.
FIG. 16. Diagram of the Boron and Selenium concentration of the Kiikiirtlii thermal Spring water at the instances between July 1999 and July 2001.
FIG. 16. Diagram of the Boron and Selenium concentration of the Kiikiirtlii thermal Spring water at the instances between July 1999 and July 2001.
FIG. 17. Diagram of the Selenium and Boron concentration of the Armutlu thermal water at the instances between July 1999 and July 2001. FIG. 15. Diagram of the Boron and Uranium concentration of the Kuzuluk thermal water at the instances between July 1999 and July 2001.
FIG. 17. Diagram of the Selenium and Boron concentration of the Armutlu thermal water at the instances between July 1999 and July 2001. FIG. 15. Diagram of the Boron and Uranium concentration of the Kuzuluk thermal water at the instances between July 1999 and July 2001.
For the waters which were already discussed in previous sections in the context of the variations of physical and chemical parameters the following variations of the tritium concentrations, as revealed by Figure 18 result: In the previous sections for several observed variations of the physical and chemical parameters a mixing process involving shallow groundwater was postulated. As tritium is a radioisotope with a short half-live of 12.4 years and enhanced concentration in the water cycle through anthropogenic production by atmospheric nuclear explosions since the 1960-ies it is mainly applied to detect young, shallow water components in deep waters of long residence time as e.g. the thermal waters. Therefore an increase of a shallow water mixing component in thermal water of long residence time (and normally with tritium contents at the detection limit should also be reflected by an increase of the measured tritium concentrations.
For the waters which were already discussed in previous sections in the context of the variations of physical and chemical parameters the following variations of the tritium concentrations, as revealed by Figure 18 result: In the previous sections for several observed variations of the physical and chemical parameters a mixing process involving shallow groundwater was postulated. As tritium is a radioisotope with a short half-live of 12.4 years and enhanced concentration in the water cycle through anthropogenic production by atmospheric nuclear explosions since the 1960-ies it is mainly applied to detect young, shallow water components in deep waters of long residence time as e.g. the thermal waters. Therefore an increase of a shallow water mixing component in thermal water of long residence time (and normally with tritium contents at the detection limit should also be reflected by an increase of the measured tritium concentrations.
water rock interaction at higher temperatures) and (ii) a water of lower temperature of local infiltration at deeper ranges of Mt. Uludag, with therefore more enriched 5°H values and corresponding 5'*O values of the recharge conditions, but which are not affected by this water rock interaction process, and therefore are more depleted in 8'%O as represented by the 8°H/3'*O diagram on Figure 23 [8][10][9]. FIG. 19. Diagram of 6H versus 6'°O values of the water of the Kiikiirtlii thermal spring for the individual sampling events.
water rock interaction at higher temperatures) and (ii) a water of lower temperature of local infiltration at deeper ranges of Mt. Uludag, with therefore more enriched 5°H values and corresponding 5'*O values of the recharge conditions, but which are not affected by this water rock interaction process, and therefore are more depleted in 8'%O as represented by the 8°H/3'*O diagram on Figure 23 [8][10][9]. FIG. 19. Diagram of 6H versus 6'°O values of the water of the Kiikiirtlii thermal spring for the individual sampling events.
FIG. 21. Diagram of 5H versus 6'°O values of the water of the Vakif Bahcge thermal spring for the individual sampling events.
FIG. 21. Diagram of 5H versus 6'°O values of the water of the Vakif Bahcge thermal spring for the individual sampling events.
FIG. 20. Diagram of the of the &°H and 6'°O values of the water of the Kiikiirtlii thermal spring versus the individual sampling events.
FIG. 20. Diagram of the of the &°H and 6'°O values of the water of the Kiikiirtlii thermal spring versus the individual sampling events.
The increase of sulphate concentration between the sample of 5.9.1989 to the sample of 9.7.1999 and the following sudden decrease to the concentration of the sample of 6.10.1999 is also related to that mixing processes induced by the tectonic activity. This decrease in sulphate concentration just after the occurrence of the Izmit earthquake indicate a dilution by a water with lower sulphate concentration but containing sulphates of the same origin. Such a dilution may be due to infiltration of lower mineralized water as were analysed at the springs of the crystalline outcrops of Mt. Uludag [10].
The increase of sulphate concentration between the sample of 5.9.1989 to the sample of 9.7.1999 and the following sudden decrease to the concentration of the sample of 6.10.1999 is also related to that mixing processes induced by the tectonic activity. This decrease in sulphate concentration just after the occurrence of the Izmit earthquake indicate a dilution by a water with lower sulphate concentration but containing sulphates of the same origin. Such a dilution may be due to infiltration of lower mineralized water as were analysed at the springs of the crystalline outcrops of Mt. Uludag [10].
Within the system of dissolved inorganic carbon (TDIC) in groundwater three different types of interaction between the dissolved species of inorganic carbon and the carbonate minerals (mainly calcites within crystalline rock environments, respectively calcite and dolomite in sedimentary rock environments) and gaseous or dissolved CO, have to be considered [13][3]:
Within the system of dissolved inorganic carbon (TDIC) in groundwater three different types of interaction between the dissolved species of inorganic carbon and the carbonate minerals (mainly calcites within crystalline rock environments, respectively calcite and dolomite in sedimentary rock environments) and gaseous or dissolved CO, have to be considered [13][3]:
These results demonstrate that the 8!3C values of the total inorganic carbon are a quite sensitiv indicator of the effect of changing conditions of the CO, sources. FIG. 40. Diagram of the resulting 6’°C values of the equilibrium CO, according to the application of the open system approach (isotopic equilibrium with the CO2 gas phase) for the investigated thermal and mineral waters of Bursa Kiikiirtli, Armultlu, Kuzuluk mineral spring and Kuzuluk thermal boreholeK3/K4.
These results demonstrate that the 8!3C values of the total inorganic carbon are a quite sensitiv indicator of the effect of changing conditions of the CO, sources. FIG. 40. Diagram of the resulting 6’°C values of the equilibrium CO, according to the application of the open system approach (isotopic equilibrium with the CO2 gas phase) for the investigated thermal and mineral waters of Bursa Kiikiirtli, Armultlu, Kuzuluk mineral spring and Kuzuluk thermal boreholeK3/K4.
FIG. 41. Diagram of the resulting 5'°C values of the equilibrium CO, according to the application of the open system approach (isotopic equilibrium with the CO2 gas phase) for the investigated thermal waters of Yalova, Gemlik, Cekirge Havuzlupark and Cekirge Vakif Bahce spring.
FIG. 41. Diagram of the resulting 5'°C values of the equilibrium CO, according to the application of the open system approach (isotopic equilibrium with the CO2 gas phase) for the investigated thermal waters of Yalova, Gemlik, Cekirge Havuzlupark and Cekirge Vakif Bahce spring.
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