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Anonymous users2024-02-10Table 4-4 lists the stable isotope data of hydrogen and oxygen and 3h and 14c of bedrock geothermal water, as well as the average values of hydrogen and oxygen stable isotopes of atmospheric precipitation, shallow groundwater and tertiary hot water in Tianjin.
Table 4-4 Isotope content of groundwater hot water.
Figure 4-5 shows the stable isotope relationship between hydrogen and oxygen for groundwater hot water, and for comparison, the data points of Tertiary hot water, atmospheric precipitation and shallow groundwater are also plotted. The δd value of atmospheric precipitation in Tianjin is ,δ18
The value of 0 is , and its average data point falls on the Craig atmospheric precipitation line (δd=8δ18).
0+10). The ΔD values of shallow groundwater are 70 65 and 18
A value of 0 is 10 and their number points fall lower to the right near the atmospheric precipitation line. In Tianjin, whether it is the groundwater of the Tertiary thermal reservoir or the bedrock groundwater, the stable isotope composition of hydrogen and oxygen is relatively concentrated and uniform, and the variation range of δd value is δ18
The 0 value varies in the range of , where the upper limit of the ΔD value is close to that of shallow groundwater and the lower limit is slightly lower than the lower limit of shallow groundwater, as shown in Figures 3-5 for ΔD and Δ18
o The data points are distributed near and to the right of the atmospheric precipitation line, and the ΔD and Δ18 of the geothermal water
O values indicate that they are mainly ** atmospheric precipitation. At the same time, it also has the characteristics of forward drift of oxygen isotopes, indicating that the water-rock reaction and water-rock oxygen isotope exchange occur in the deep buried and high-temperature state of underground hot water.
Bedrock geothermal water, whether Ordovician, Cambrian, or Miocoberozoic thermal reservoirs, δd and δ18
The o-values are all very close and, combined with their distribution conditions, seem to indicate that they are distributed and circulated in the same geothermal water system. In addition, the ΔD value of the groundwater is about 10 15 lower than that of the cold water in the open ground, and if the ΔD value decreases for every 100m increase in the sea dial, the sea dial in the recharge area should be 400 600m higher than that in this area, indicating that the recharge of the geothermal water comes from the northern mountainous area.
Radioisotope 3 of geothermal water
The highest and lowest values of h concentration are significantly lower than the background 3h concentration of local atmospheric precipitation and surface water, so the age of groundwater is still relatively old compared with the atmospheric precipitation value of the same period in the region.
14 of the groundwater hot water
c. Age is determined and passed by 13
c The preliminary understanding obtained after correction is that the age of bedrock groundwater is about 10,000 years, and there is a gradual aging trend of groundwater from north-east to south-west, indicating that the groundwater is slowly runoff from north-east to south-west after being recharged by atmospheric precipitation infiltration from the northern mountainous areas, which belongs to the deep circulation water originating from atmospheric precipitation.
Figure 4-5 Stable isotope relationship between hydrogen and oxygen in groundwater in Tianjin.
1—Mean atmospheric precipitation 2—Shallow groundwater 3—Hot water in Tertiary thermal reservoirs 4—Hot water in Ordovician thermal reservoirs 5—Hot water in Hanhu Qiansuowu thermal reservoirs 6—Hot water in Meso-Neoproterozoic thermal reservoirs.
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