CONSTRUCTION GEOLOGY np Prague 1 – Gorkého nám. 7
Task name: Bílina - protective zones
Task number: 76 177 13 GH
Prepared by: Pg. V. Cyvín
SPA HERBAL
research study
Prague, March 1977
CONTENT
I. Introduction
II. Overview of older works
III. Historical overview and development of catching
IV. Geology and structure of the territory in connection with the genesis of mineral water
V. Hydrogeological conditions
VI. Bílina mineral water, its properties and indications
VII. Chemistry of mineral water
VIII. New sources of mineral water
IX Protection of the source against unwanted interventions
X. Protection zones
XI. Design of a hydrogeological survey
XII. Conclusion
SIDE DISHES :
1. Situation of springs and wells
2. Geological map 1:25
3. Geological profile
4. Height conditions around Bílina (profile from the river)
5. Profile of Skalní pramene 1 : 50
6. The Josef spring group
7. Receiving shaft (bottom)
8. Receiving shaft (section I.)
9. Receiving shaft (section II.)
10. The bottom of the receiving shaft (cracks)
11. Bílinská kyselka (rehabilitation of springs)
12. Situation plan 1:2 880
13. Wider protection zone
14. Provisional protection zones 1:50
INTRODUCTION:
II. OVERVIEW OF OLDER WORKS
The issues of Lázní Bílina were mainly dealt with by the following authors:
C. Schwenokfeld (1607), JF Kempf (1706), W. Sparmann (1733), Ch.G.Schwenke (1752), J. Carteuser (1758), C. Troschel (1763), G. Zückert (1768), A. Cronty (1777), M. Hansa (1784), FA Reuss (1788), D. Hufeland (1815), AK Eichler (1821), W. Gerle (1821), JPKrzisch (1887), J. Löschner (1859) ), J. Lehmann (1877), EHKisch (1879, 1902), K. Theimer (1891, 1892, 1908), W. Gintl (1898), CG Laube (1898), F. Steiner (1898), K. Zima (1953, 1955), O. Hynie (1955), J. Vrba (1955), V. Myslil (1959) and G. Kačura (1959, 1964, 1967).
For the given task, all available archival documents were studied, extracted and processed, mainly from the archives of the Ministry of Health, from the Geofund and from the Central Institute of Geology. Apart from a few maps, no archival materials are available at the headquarters of the spa organization in Bílina.
The oldest significant work on Bílinská kyselka is the monograph by FA Reuss from 1788. It describes the natural (geological) conditions, history, capture of mineral springs, chemistry of min. water, its medicinal effects and indications.
AK Eichler (1821) describes the recapture of springs after their destruction in 1806 and deals with the issue of filling mineral water
JE Krzisch (1837) and G. Schmelkus (1841) state the state of capture of the four springs at the time, yield, temperature, and indications.
J. Lóschner (1879) cites older authors and deals mainly with the healing effects and chemistry of mineral water in Bílina. EH Kisch (1879, 1902) describes the geological conditions ✓ around Bílina and the history of the capture of mines. springs. The most important work on Bílinská kyselka is the publication from 1898 by W. Gintl (hydrochemistry), G. Laube (geology, hydrogeology) and F. Steiner (hydrotechnical work). The publication follows on from the remediation work carried out ✓ in the years 1888 – 1890. W. Gintl tries to find the origin of the mineralization of bilinec acid in the surrounding rocks, gneiss, bellstone and basalt. It assumes that mineral water acquires its chemical composition in cracks, especially during its exit path in the gneiss.
He analyzes the mineral water of the newly captured rock spring and compares it with older, chemical analyses. Due to the proximity of lignite seams, it is believed that the CO2 is of organic origin. Its losses during collection are explained by dilution by uncontrolled outflows of shallow waters. On the basis of his geological research, G. Laube finds that mineral water springs from fissures parallel to the schist at the western border of the gneiss, i.e. from west to east. At the turn of the century, the results of the remedial works were processed in summary articles by K. Theimer (1891, 1892, 1908) and in the collection by E. Kisch (1902), where the development of mining of mineral springs in Bílina is recorded chronologically. During the next 50 years, experts showed little interest in the existence of the spring. The Bílinské springs were monitored only marginally by the balneotechnical service of the spa organization.
It was not until 1950 that 0. Hynie and K. Zima submitted a report on the geological and hydrogeological conditions of the mineral spring in Bílina. According to their opinions, a landslide of rocks (rock masses) of Cretaceous and Tertiary age occurred in the place of the captured springs. The authors explain the low yield by the relatively small infiltration area and the small depth of the zone of formation. They consider the origin of CO2 to be juvenile, inorganic. They believe that a significant increase in the yield of mineral springs cannot be achieved here. The archival file of K. Zima (1953) deals with a hydrogeological survey of the surroundings of the town of Bílina in order to secure a new source of drinking water. Here, K. Zima describes the geological and hydrogeological conditions of the wider surroundings of Bílina and proposes exploratory hydrogeological wells in the area east of Bílina. In 1955, J. Vrba prepared a report evaluating the hydrological observations of the Bílin springs from 1941 – 1946. From the graphical representation of all the main indicators and data, it is possible to read the dependence of yield on rainfall (with an approximate three-month delay), the effect of barometric pressure on yield and a positive influence yield on the amount of CO2. In 1955, K. Zima also submitted a comprehensive report on the geological and hydrogeological conditions around Bílina, as a supplementary report to the above-mentioned report from 1950. In his work, he deals with the development of spring harvesting and the general hydrological issue of the spring. According to K. Zima, the acid formation zone is at a depth of 120 — 150 m below the junction of Mnichovce and gneiss, where the "Hibsch's Bílin fault" is apparently taking place.
In the opinion of K. Zima, the acid rises in a horizontal direction, not in a vertical direction. Finally, the author presents proposals for temporary protection zones I and II. degree and proposes the execution of 2 exploratory wells in the area north and south of the existing sump, and 2 horizontal exploratory wells from the bottom of the main sump in the NW and SW directions. In 1959, V. Myslil and G. Kačura developed a proposal for temporary protective belts, which was not preceded by a detailed survey and which is mainly based on the previous findings of older authors. The last and most comprehensive hydrogeological work on Bílinské kyselka comes from 1967 by G. Kačura. The author evaluates all older opinions and works and presents a fairly comprehensive development of the capture of sources, including their use. This work is the result of hydrogeological research from 1959-1965, which was supposed to ensure an increase in yield and mineralization of the spring.
Based on his proposal, 3 boreholes (2 oblique, 1 vertical) were drilled in the area of the spa. These wells will be discussed in more detail in Chapter VIII. G. Kačura performed a detailed analysis of the system of cracks that could bring acid to the surface. From the study of the receiving shaft, he concludes that the predominant direction of the open fissures leading the mineral water is the h 2 direction. According to G. Kačura, this main direction is therefore decisive for the output phase of the acid in the subsurface part of the crystallinic. Unlike O. Hynia and K. Zima, he is inclined to the opinion that CO2 is more of a vadose origin. G. Kačura also deals with regime relations at springs and wells. It first measures the springs in the receiving shaft before the springs are affected by the new wells. He divides the springs into two groups according to their richness. The deep sump capture method and adjustable shallow capture below the reduced water level allowed that neither the gasification value nor the bicarbonate content changed during the year.
The balance between acidic and shallow waters was regulated by changes in the withdrawal amount, which were reflected in the discharge height of the water levels. The levels then reacted simultaneously with changes in the CO2 content. 41, :- .“gmeters in water level movements were caused by inappropriate capture of the spring. Only at the Ruschel spring did the higher CO2 content cause a simultaneous decrease in the level. It was only during pumping tests on new wells that the regime of the original springs was disturbed. When pumping from the entire heavily gassed section in the new well V 1 (42,00 — 128,50 m), a continuous decrease in yield and CO2 content occurred in all springs. The quantitative ratio between the withdrawal at the V – 1 well and the old springs was this: if the withdrawal did not exceed 10 1/min and therefore the reach of the depression did not reduce the discharge height of the springs in the shaft, then it was also possible to take approx. 10 1/min in the sump. Despite some unclear circumstances regarding the genesis and regime of the source, this work should be considered fundamental and a starting point for further research and exploration work.
III. HISTORICAL OVERVIEW AND DEVELOPMENT OF TAKING BÍLINÍS KÍSLÍKA
The Bílin spring is one of the oldest and best-known natural healing sources in Bohemia. Mineral water is used both for medicinal purposes (drinking barks, inhalation, baths), on the one hand, it is popular as table water. It has been bottled since 1781. Although the official discovery of the springs is attributed to the owner of the estate Eleonora Lobkowitz in 1712, their occurrence was probably known much earlier. This is evidenced, for example, by the mention in the Chronicle of Václav Hájek from Libočany, cited by authors from the 17th century to the present day. G. Kačura quotes W. Sparmann, who states in 1733, "that D. Zittmann introduced drinking barks with Bílina acid and rabbit water a few years ago". This water was brought to Teplice for use in spas.
The spa physician FA Reuss had great merit in preserving the source for the therapeutic indications. He writes the first monograph on the Bílin spring and from the 80s he becomes an influential adviser to the Lobkowitz family. In the second half of the 18th century, the period of mail order service of mineral water in special jugs begins. Josef Vilém Löschner gives the exact number of jugs sent out. In 18, 1779 jugs were distributed, in 9.144 already 1786 and in 42 even 000. At the turn of the century, shallow mineral springs mixed with plain water, mostly surface water, and in 1856 they were almost destroyed by torrential waters.
Under Prince Franz Josef Lobkowitz, three new springs were discovered near the original four springs. Josef's, Karolin's and municipal. They were shallow sumps with a maximum depth of 3 m. The first serious reconstruction of the sump pit took place in 1852, when drainages were excavated to remove surface water. The mineral water evaporated in the pans and mixed with the bitter water from Zaječice. The resulting product was then sent to Teplice. In 1871, the Moritz spring was discovered and a spa house was built. Significant progress in the reconstruction of the wells and the entire collection system is represented by the works carried out in the years 1880-1890, designed by W. Gintl, CG Laube and F. Steiner.
They are described in the monograph "Die Mineralwasser quellen von Bilin in Böhmen und die an denselben in den Jahren 1888 - 1890 durchgerůhrten Sanirungs - Arbeiten". It was about ensuring greater abundance and mineralization. CG Laube suggested mining by either shaft or borehole. The work was directed by engineer F. Steiner, who carried out 16 dug probes down to the granite bedrock (approx. 22,4 m deep). The probes were connected by a connecting tunnel. A receiving shaft was established in the place of the most mineralized acid. This is how the so-called Rock spring (between probe XIII and XVI), which became the basis of future mining. Its yield was 14,4 m3/day. acid and weakly mineralized waters were discharged separately through the tunnel.
At the same time, a 12 m deep probe, a 16-20 m deep borehole and later a 130 m deep borehole were also carried out at the ČSD station. The source was later called the Fr spring. Joseph. Further rehabilitation work was carried out by A. Scherer. Etc and the weathered surface of the bedrock was exposed. A total of approx. 155.000 m3 of rock was removed in an effort to drain the pits. Thus, a deep break was created in the gneiss, in which 4 pits and notches were created following the cracks and ridges of the chert in the gneiss. (Q = 13,8 1/min).
However, the desired stabilization of the regime was not achieved, and the yield and concentration gradually decreased. In the years 1913 – 1914, further rehabilitation work was therefore undertaken. The cuts were extended into the slope (to the west) and deepened up to elevation 205,615 (6 m lower). A 26 m deep construction pit with dimensions of 18 x 9 m was created. It was then bricked as definitive. In addition to dry CO2, the following were captured by the pit: 1) Main rock springs, 2) SW north of them, 3) NE in the northeast corner of the pit, 4) exits "C", 5) in the southern part "R", 6) in the SW corner " AND". Strands 1 – 3 were used for spinning. In the years 1922 – 1932, all springs showed a downward trend again. This prompted the spring inspector from Karlovy Vary, Ing. Packert to the fact that he had set up the so-called an irrigation shaft "as a regulator of the balance of underground water", situated 43 m above the main sump. It was 16 m deep and 3 shallow wells were excavated in its bottom to a depth of just over 20 m. When the yield decreased again due to the dry years of 1933-34, the total yield was 5,8 1/min.
In 1935, the withdrawal of the main springs P + Q was reduced by establishing a channel in the bottom of the shaft. The output was increased to 6,3 1/min (1937). This measure did not have a lasting effect, and it was therefore necessary to further reduce the pit, taking into account the oblique course of the cracks. The final dimensions of the sump were 9 x 4 m, up to an elevation of 199,60 m above sea level, 6 m lower than in 1914 (2 m above the bottom of the Bílina stream). The reconstruction was only completed in 1939. The construction pit was then deepened by a total of 8 m from the original bottom with the bottom at a height of 197,51 m. A. Scherer justified the deepening by the slanting of cracks. He considered it a long-term measure. The deposits were found at a lower level - further south. The main eruptions P + Q approached each other and showed a double occurrence, i.e. P + Q I. and P + Q II. They were connected by a horizontal pipe and served as the main source for bottling. Their combined yield was 4,86 1/min. The other sources were reflected in the new catchment level in a completely different way. In the northern well, the Ruschel - quelle spring (Q = 0,53 1/min) was captured from the long joint, and the Sohlenquelle (so-called Floor) with a yield of 0,36 1/min was captured at the bottom of the shaft. In addition, two less mineralized springs ran from the bottom and from the wall, which were not collected, namely Decken-quelle (ceiling) (Q = 0,20 1/min) and Wandquelle (wall) (Q = 5,45 1/min.) . In the southern wall (continuation of the P + Q fissure), seepage A (Q = 0,33 1/min) was collected. At first, the higher concentration of the main springs decreased after the end of collecting, as a result of long-lasting rains.
Yield of springs (June 1941)
1) Ruschelquelle 7,1 1/min. 2) Sohlenquelle 1,5 1/min. 3) Wand and Deckenquelle 1,0 1/min. 4) Secondary strands A 0,25 1/min. 5) R 2,01 1/min. 6) CO (dry)
Other mineral springs were not measured at that time.
Analysis of mineral water from 1940
Evaporator 4 mg/675 Cl. 1 mg/202 1- 5024 mg/605 HCO1 3 mg/3 CO938 total 1 mg/2 CO4 free 410 mg/1
In the opinion of E. Wollmann (1941) it is stated that the removal of a large amount of soil and a deep intervention in the gneiss bedrock was an unfavorable moment for the regime of mineral water. He proposed to lead a 200 m long tunnel from the yard of the pine mill with a gradient of 1:100, which would lead up to a height of 209 m above sea level and bring min. water with CO2 for collection. However, this proposal was not implemented.
Measurement in 1943
Main springs 7,35 1/min. Ruschelquelle 2,14 1/min. (pinning room)
A total of 110 – 120 hl/min was brewed. water.
In 1944, the Deckenquelle was also connected with a flow rate of approx. 1,01 l/min. So the remaining Sohlen and Wandquelle and the side springs A, C and R, which had a small capacity, remained uncaught. At that time, the spring vase at the Josef spring was also abolished and a storage tank for mineral water was established in its place. In 1, attempts were made to ensure that the sourdough did not lose CO1945' during accumulation, but it took 2 years (7) for the realization of a special storage tank. Instead of the old wooden structure above the spring pit, the main pit was covered with an iron structure.
IV. GEOLOGY AND STRUCTURE OF DZELD IN CONNECTION WITH THE GENESIS OF MINERAL WATER
The investigated area is located at the western edge of the Český středohoří. Here, the Bílina River cuts into gneiss bedrock with overlying Cretaceous, Tertiary, and Quaternary sediments. All sediments are intruded by Tertiary volcanics (basalts and cherts). In the vicinity are the hills Bořeň (531 m), Železný vrch (455 m), Kaňkov (436 m), Kačíkov (398 m) and Mnichovec (380 m above sea level). The subsidence field of Cretaceous and Tertiary strata was flooded in the Miocene. This is how the lignite seams of the Mostecka Basin were formed. The Miocene basin north of the Bilinek fault has a different thickness due to subsidence and tectonic unrest. However, younger movements were also important - mainly on the Bílin fault.
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According to K. Zima, the output of the acid is closely connected with the waters that infiltrate into the permeable and weathered surface rocks. During the history of the Bílina spring, these waters influenced the mineralization of the captured acid. The zone of acid formation should be sought deeper on permeable gneiss fractures. According to more recent authors (Hynie, Zima), CO2 is of juvenile origin. Its occurrence is usually associated with volcanic activity. In the latest work, G. Kačura considers the origin of CO2 to be vadgistic. These completely contradictory views will need to be clarified by further research. Mineralized fissure water, gasified 002, emerges through permeable fissures to the surface on the left western bank of the river Bílina. The very fact that mineral water and mainly CO2 emerge only on the slope of the Bílina valley indicates that the tectonic line running through the Bílina valley is impermeable sealed by clayey rocks. The place where the mineral water is created is located west of Bílina. K. Zima believes that the original natural spring and today's capture of the spring are 2-1 1/1 km away from the CO2 outlet. The actual zone of CO2 formation probably lies under the contact of basaltic rocks with gneiss. Allegedly, this is where the protein disorder takes place (J. Hibsch). During the spring's existence, its remediation was checked several times (see above), not always with a positive result. Only the last radical intervention (establishment of a huge sump 18 x 9 m) isolated the spring from simple surface and shallow underground waters. Bal-4otechnically, the acid is captured almost perfectly, so there is no need for objects or the method of capture
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measures (Hynie - Winter 1950). G. Kačura, on the other hand, draws attention to some of its shortcomings in the case of the central sump: difficult separation of differently mineralized waters, the easy possibility of influence of the received waters by atmospheric factors, and the difficulty of preventing CO2 leakage outside the receiving system. The temperature of the captured mineral water varies from 10 to 11°C. The outlet of the spring at the point of collection is not vertical. The zone of CO2 formation is roughly horizontal at a depth of 120 – 150 m. Therefore, the thrust of the acid is from the west along the tectonic fault lines in the E – W direction. Despite some ambiguities, it is clear that the place of formation is bound to a fault zone (Bílin fault) and that the exit of juvenile CO2 takes place along the exit paths of eruptive Tertiary rocks.
V. HYDROGEOLOGICAL CONDITIONS
The crystalline rock base (double-mica gneiss) forms one regional unit with the sedimentary cover (chalk, Tertiary).
CRYSTALLINICUM
The gneiss is relatively impermeable, but numerous fissures and mainly larger faults of tectonic origin allow the movement of infiltrated rainwater or water that is transferred to the bedrock by permeable cover rocks. In larger fault zones, there is a greater concentration of fissure waters, which drain by gravity to lower positions and, under favorable morphological and geological conditions, can either form a spring gush or pour out into the surface flow at the bottom of the valley. Waters sinking to greater depths and gassed with CO2 give rise to acid lakes located southwest of the town of Bíliny.
To the east of the Bílina valley, where the protection zone no longer extends, the terrain is characteristically divided by two morphologically distinct valleys. It is the Žižkov valley from Razice and Kučlín, where the Syčivka stream flows, and the valley from Lukovo and Radovesice and the Lukovským stream. According to hydrological observations, the average annual discharge of Syčivka is 7 1/vt. and Lukovského potok 69 l/vt. The specific runoff (area of both basins approx. 24 km2) is 0,5 1/s/km2. This low value corresponds to numbers derived from other gneiss territories. Observations of stream flows are important knowledge for further evaluation of the gneiss area. According to measurements from April 1953, the flow on the Lukovský stream below Radovesice was 12,04 1/s and below 18,76 1/8, Žižkov() valley 20,09 1/s. In the extension of the line from Radovesice to the WNW leading along the northern foot of the Chlum, a wider area becomes wet, and it is quite likely that fissure waters drained by a tectonic fault are pouring out here.
SEDIMENTARY ROCKS
The crystalline sedimentary mantle includes: a) Upper Cretaceous deposits and b) Tertiary deposits.
ad a) Remains of the lowest zone II belong to the Cretaceous formation. (Cenomanian) in the reef facies, preserved on a gneiss substrate, approximately on the line Liběřice – Lyskovice. 0enomanian is developed here by coastal sediments, i.e. aggregates with lime putty. They do not have a great power (max. 20 m), but they are impermeable. Elsewhere, the Cenomanian is developed as sandy shales and firm fine- and coarse-grained sandstones. Even these rocks are not hydrogeologically favorable. The higher chalk zones are made up mostly of clayey and silty rocks (turon), impermeable to water. The only hydrogeologically favorable rock here may be Cenomanian sandstones with permeable cement. However, they are very limited in development. It depends on the strength and slope of the aquifers. The structural and hydrogeological conditions are best clarified by the geological profile leading from Bílina through the valley of Lukovského potok SE towards Lukov (appendix No. 3).
ad b) Tertiary sediments include, on the one hand, Oligocene clays and sands deposited on the chalk layers SE and E of Bílina, on the other hand, Oligocene and Miocene clays and sands. filling the depression west and north of Bílina, already belonging to the Mostec lignite basin. The Tertiary sediments in the overburden of the chalk layers do not come into consideration for collecting a large amount of underground water. More favorable hydrogeological conditions are created only where the Oligocene sands allow greater infiltration of rainwater, which here runs down the impermeable clay subsoil and springs up as stratified springs.
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In the lignite basin, flowing sands of considerable abundance were encountered several times during the openings. However, from a water-related point of view, these mine waters are not suitable for drinking purposes even after treatment. They have considerable hardness and inappropriate mineralization (manganese, sulfates) and are often bacteriologically objectionable. Hydrogeologically, this aquifer is tied to the positions of sands of smaller sizes with an irregular area. Most often, sands form lenticular positions in the middle of clays with poor replenishment of water reserves, so that after depletion, the yield decreases. Shallow Quaternary waters can be used mainly from the alluvium of the Bílina River (gravel sand). Clarification of geological and hydrogeological conditions in the wider area. Bíliny would require a larger number of wells dug into the subsoil. The bearing wells, realized for the purposes of SHD, provide the required data on the oil zones, or their equivalents, while the hydrogeological documentation is completely insufficient.
VI. BÍLINSKÁ KYSELKA, ITS PROPERTIES AND INDICATIONS
Bílinská is the strongest and most valuable pure alkaline acid in Bohemia. It is completely clear without smell and color, strongly sparkling, pleasant taste. Bílinská mineral water has a relatively stable chemical composition, it is bacteriologically harmless. It is filled in its original state, without any modifications or additives. The bottles are closed with crown caps and a cork disc and a tin insert.
The curative effects of bilinsk acid are mainly caused by acidic sodium carbonate, lithium carbonate and carbon dioxide.
The properties of alkaline salts are twofold: they dissolve mucus and neutralize acid. Dissolving phlegm comes into consideration in the case of inflammation of the respiratory tract (either by drinking warm acid, or by inhalation) as well as in stomach and intestinal diseases. A special building is set up in the spa for inhalations.
The alkalizing effect that occurs after the absorption of mineral water is also used with success in diseases of the digestive organs caused by hypersecretion and hyperacidity, then in catarrh of the renal pelvis, bladder, and urethra, when the acidity of the urine decreases and the formation of sand and stones stops. Even in these cases, you can count on the dissolving properties of sodium and increased excretion of urine, which reduces its concentration and washes out smaller stones. In other metabolic disorders, such as gout, the effect of bilic acid is explained by the easier solubility of uric acid by alkalis, sodium and lithium.
Lithium's function as a uric acid solvent is known to provide significant pain relief. Another, beneficial effect is also regular and frequent drinking of acid, which removes uric acid from the tissues mechanically. In case of diabetes, Bílina mineral water lowers the blood sugar level and works well in combating diabetic acidity by increasing the alkali reserve in the blood. In chronic catarrhs of the stomach, albuminous acid, when warm, binds excess stomach acid. Drinking cold soda, on the other hand, stimulates the stomach, which excretes an increased amount of acid due to carbonic acid. For these diseases, the professional indication of a doctor is therefore important.
Carbon dioxide (in addition to its refreshing taste) directly stimulates the gastric mucosa, which, by excreting hydrochloric acid, supports the activity of the stomach. Congestion of the gastric mucosa promotes water absorption and increases urine excretion. Both are valuable in the medicinal use of sorrel. In this way, substances dissolved in mineral water are brought quickly to the tissues and harmful substances are removed. The carbon dioxide content of the stomach does not bloat or exert harmful pressure on the heart.
Since 1847, lozenges have been made from the salts obtained by evaporating acid. They are most often used in gastric catarrhs with increased acid formation, in acid belching, heartburn, as well as in constitutional diseases of the glands and bones and in respiratory tract catarrhs. Whitening pastilles are also indicated for infants, if children cannot tolerate fat and if they get diarrhea after a milk diet.
VII. CHEMISTRY OF MINERAL WATER
Bílinská mineral water is a cold pure alkaline acid. It has 7 mg/kg of dissolved solids, over 300 mg/2 of free CO300 and a temperature of 1°C.
The first chemical analysis was carried out in 1786 by J. Berzelius. Since then, we have no evidence of the analysis carried out from the entire 19th century until the 20s of our era. A rare preserved exception is the analysis of prof. Eng. Gintla from 1908. But even these data cannot be compared with more recent ones, because on the one hand it is an analysis of a mixture of captured acids and on the other hand a single spring or other mixture of unspecified mineral water. We know from history that the mineralization of Bílina water rose or fell according to the amount of vadose or auto waters that were mixed with mineral water. There was also a period when the collection of water was completely impossible (1800 – 1806). Previous administrators and users of springs did not pay enough attention to their regular monitoring. It follows that we do not actually have a single certificate or a copy of it from the 18th or 19th century, so that we can assess the hydrochemical data with newer ones. And the current analyzes following only basic indicators definitely do not give the overall chemical picture of mineral water.
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Analysis by Eng. Gintl
(4 as standard for bile acid - from 1908) pH alkalinity m val/1 mg/1 6,2 – 58,2 millimoles – – (new standard -1963) mg/1 V-1 V-3 – – – -Na- 1 749,0 75,90 1757 1378 K- 88,89 2 270,0 85,3 92,4 Li+ 3,79 0,564 3,8 4,1 N114+ 0,00 – 3,1 3,8 Ca2+ 151,5 3 789 172,8 Mg164,5+ 2 50,6 2 077 Dan50,8+ 50,4 2 0,06 0,001 Fe0,08+ 0,17 2 1,66 0,028 P- 1,4, 1,3 1,2 0,063 5,0 Cl- 4,5 228,3 6 441 229,4 NO226,8- 3 0,0 0,0 n0,0- 02 0,0 0,0 HCO0,0- 3 4 383,0 71 850 4 418,0 4387,0- 5042 587,1 6 118 575,0 H591,3iO28 3 O 54,91 700 40,0 CO73,7 free 2 2 317,00 52,66 2 505
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If it was a pine mill, compliance with the criteria for total mineralization was very strict. Only mineral water with evaporation higher than 4 g/1 was bottled; otherwise bottling was aborted. Based on the regime data, it was clear that the higher the yield of the spring, the greater its mineralization. In general, it can be said that abundance and mineralization had a downward trend. Always after successful remediation works, the mineralization increased and then gradually decreased together with the yield. And due to the fact that ✓ currently only five values are monitored in the chemistry of bilinsk acid (table no. IV), namely Mg2+, Ca2+, Cl, HCO3 and free CO2, we cannot even cover all the differences in the ✓ chemistry.
According to Table No. II, the lowest mineralization ✓ was in the main sump and in the pinnery in October 1929 (at the limit of 4.000 mg/1); on the contrary, the highest was in December 1940 (over 4.600 mg/1). In the comparison of the analyzes of the older date with the newer ones, there is a noticeable difference in chemistry (analyses 59 – 63) in favor of the mineralization of the most recently executed and taken wells V1 (for the pine mill) and V3 (for the spa). More detailed data on these wells are given in the work of G. Kačura from 1967 (e.g. in the chemistry of water leaching of gneiss, G. Kačura infers the genetic significance of gneiss for the formation of acid rock. According to the analysis of gases – 02, N2, A, he considers part of CO2 to be vadose In any case, it must be emphasized again that the current analyzes are completely insufficient and, given the importance of the spa, it would be necessary to carry out chemical analyzes of the water of both sources at least once every 2 months.
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2AWII.KA No. 1.4 Chemical analyzes min. Water in the main tank.aav pinit-né Number Day of sampling euěin at 1100C 002 total CO2 semi-bound CO2 free hl. sump pinnir I hl. jimka pinírna hl. jimka pinírna hl. jimka pinirna 1 2 3 4 5 6 7 8 9 10 1 1.7.1924 4.758 4.603 1.185 1.176•,2 2.1 1924 4.118 4.115 4.253 4.139 1.188 1.188 1.877. 1.763/3/11.12.1924 4.142 4.125 i 1.188 1.161 4. 31.1.1925/4.046/4.049 4.299 4.136 : 1.188 1.188 1.923 1.760 5 30.6.1925 4.204. 4.197 4.462 4.450 1.248 1.243 1.966 1.964 6 3.12.1925 4.356. 4.350 4.659 4.652 1.287 1.292 2.085 2.068 7 5.5.1926 4.075. 4.089/4.285/4.299 1.193 1.193 1.899 1,913 8 31.8.1926 3.932 3.928 4.127. 4.139 1.171 1.171 1.785 1.771 9 1.7.1927 3.770 3.760 3.888. 3.853 1.089 1.089 1.710 1.675 10 25.10.1929 4.027 4.008 4.272. 4.198/1.177/1.177 1.918 1.844 11 14.2.1930 4.125 4.122 4.422 4.411 1,221 and 1.216/1.980/1,979 12 2.3.1932 4.575 4.560 4.640 4.613 1.310 1.310 2.020. 1.993 13 14 17.10.1932 7.3.1933 4.420 4.522 4.408 4.508. 4.650. 4.791 4.628 to 1.155 1.155 4.765 1.353 1.353 2.340 2.085 2.318 2.059 15 5.12.1933 4.545 4.435 4.971 4.850 ro 1.338 o's 1.338 2.295 2.174 16 13.3.1934 4.520 4.544 4.900 4.880 1.388/1.388/2.124 2.104 17 29.6.1934 4.532 4.460 4.750 4.702 1.328 1.328/26094/2.046 18 13.11.1934 4.332 4.452 4.702 4.725 1,319 1.319 2.064 2.087/19/19.2.1935/4.464 4.428 4.728 4.715 1.318 1.318 2.092 2.079 20 14.11.1935/4.272/4.240/4.410 4.385 1.298 1.298 1.814 1.789 21 2.7.1936 4.200 4.185. 4.290 4.270 1.243 1.238 1.804 1.794 22 17.2.1937 4.175 4.190. . 4.260/4.280/1.284 1.280 1.692 1.720 23 17.7.1937 3.760 3.755 1.020 3.960 and 1.130/1.130/1.760 1.700 24 16.9.1938 4.790 5.080 5.180 4.990 1.540 1.540 2.100/2.910/25 5.3.1940 4.410 4.460 4.780 4.620 1.360 1.360 2.060 1.900/26/16.7.1940 4.420 4.420 4.800 4.670 1.330 1.300 2.140 2.010 27 5.12.1940 4.675 4.665 4,410 4.380 1.420 1.420 1.570 1.540 28 4 27.8.1941 4.308 4.313 4.422 4.367 1.280. 1.280 1.860 1.810 29 9.1.1943 2.320 2.300 30 29.6.1943 2.343. 2.269 31 8.12.1947 2.340 2.290 32 1105.1944 2.364 2.295 33 4.9.1943 20341 XNUMX XNUMX. XNUMX XNUMX XNUMX XNUMX XNUMX XNUMX XNUMX. XNUMX ■•• XNUMX XNUMX XNUMX. XNUMX •••■ XNUMX
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Pghračovani table b ul kyS21 Cítilo Day of cdběr Cl- mg / 1 S02- / 1 mg DC0- mg / 1 C1-+ SO + SCC 3 hl. sump and powder room hl. sump pinnir hl. sump pinirna i hl. jimka sawmill 2 11 12 13 14 15 i 16 17 18 1. 1.7.1924 2. 2.10.1924 3.294 3. 11.12.1924 em 3,294 4. 31.1.1925 fth. 3,294 5. 30.6.1925 3.461 6. 3.12.1925 3.569 7. 5.5.1926 3.308 8. 31.8.1926 3.247 9. 1.7.1927 3.020 10. 25.10.1929 3.036 11 14.2.1930 3.386 12. 2.3.1932 3.633 13. 17.10.1932 184 600 3.203 i 3.987 14. 7,3.1933 3.752 15. 5.12.1933 3.710 16. 13.3.1934 3.710 17. 29.6.1934 3.683 18. 13.11.1934 3.658 !in 19 19.2.1935. 3.655/20/14.11.1935 184 . . . 184. 603 598 3.599 3,599 4.386 4.381 21 2.7.1936 183 183 594 594 3.447 3.433 4.224 4.210 22 17.2.1937. 185 185 592 592 3.561 3.549 4.338 4.326 23 7.7.1937/162/162 521 521 3.133 3.133 3.816 3.816 24 16.9.1938 226/223/627 624 4.270 4.270 5.123 5.117 25 5.3.1940 190/190/605 609 3.771 3.771 4.566 4.570 26 16.7.1940 187 187/605/608 3.688 3.688 4.480 4.483 27 5.12.1940 202 202 605/608/3.938 3.938 4.745 4.748 28 27.8.1941 182 182 589 589 3.650 3.550 4.321 4.321 290 9.1.1943 227 585 4.340 5.152 30 29.6.1943 227 – 594 -4.372, 5.193 31 8.12.1943-227 597 – 4.404 . 5.229 December 32, 11.5.1944 229 579. 4.446. 5.255e 33/4.9.1944/227 591 4.331. 5.150. XNUMX. XNUMX XNUMX XNUMX XNUMX with XNUMX ..
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TABLE NO. III Chemical analyzes of springs min. of water (of recent date; i N 3 I 05 1 2 3 4 Date cdbCzech Republic 6 16.6.1959 8.2.1966 21.4.1961 36.6.1960 21,4,1961 pil 21.4.1961 6,2,, 1,) 3 6,5 .6,35 6,1 cdparks at 110 mg/1 4.260 5.656,0 4.546,4 4.565,6 4.386,8 3.600,8 alkalinity mval/1 58,52 64,75 62,50 68,1 50,9 45,7 mdl K' Lit Nh4Cu2+ ,; 24. kn2+ Cl- 1463 N6„- liCC,3 6042- ii,biGi C62(vol) 1.447,0 bs,b 2,20 0,6 132,2 56,6 0,619 1,63 1,15 163,4 0,0 1.571.C 599,9 94,3 2.542,6 1,568,7 101,7 3,1 6,6 151,7 49,2 0,0 0,3 4,55 266,4 0,0 0,0 3.012,5 612,7 49,9 2.252,6, 1,605,5 0,6 128,7 48,14 3,12 186,0 0,6 0,0 4.134,1 606,28 2.455,0 1.628,6 1 8,68e16,18 1,2 218,0 6,6 0,0 4.154,1 524,17 2.308,0, 1.550,2 – 136,55 51,34 – 3,3 182,0 6,0 6,0 3.553,9 610,99 2.372,0 1.1140,8 – 105,82 46,49 – 2,79 132,0 0,0 0,0 2.767,7, 532,71 2.0194 XNUMX XNUMX XNUMX
1/ 3M:'.3 m, water for pine mill (1959 OX), 2/ Runchel spring (19601 , 3/ Io+II spring (1961), 4/ Ft0 spring (19b0), i/ PodlaZai spring (1961), 6/ ..;tnovy pramen (1961), 7/ Ceiling spring (1961), 8/ spring A (1961). geologically; sample 9-1962 annulus of the development center of West Bohemian Springs; sample 10 – analysis of the Research Institute for Physiatry, Balneology and Climatology.
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Continuation of Table III
I 7 8 9 10 11 1 12 1 sampling date 24.4.1961/21.4.1961/31.8.1962 -I 12.11.1963/26.7.1962/19.1.1963 6,5/6,55/6,7 J 6,45/110/1 4.269,2/3.688,4/1.150,0 – 5.017,00/1/1 : pH 59,1 51,2 11,5 72,39 – – evaporation at 75,24°C mg/73,8 1 4 2 2 – – alkalinity mya2/2 3 2 3 5042 2 3 Nar mg/2 K Lig NH1.527,2+ ca111,5+ Mg49,64+ 4,01 kn+ Ne177,0+ F Cl NO0,0- NO0,0 HCO3.605,1 596,47- H2.293,00SiO1.384,6 CO101,53 (vol) 41,3 – – 2,45 144,0 – 0,0 – 0,0 3.023,2 529,63 1.781,0 0,0 – 108,0 47,74 – – – 0,0, 33,6 2,0 – 0,0 – 701,5 345,2 1.757 4 85,3 – 3,78 – – 3,1 172,8 50,8 – 0,078 – 1,38 4,96 229,46 0,0 0,0 – – f I / [ ? t 4.418,1;575,0 40,0 2.505,5 1.875,0 110,5 114,8 51,6 10,9 238,9 4.591,1 587,2 58,0 1 2.234,0 1.810,0 108,2 ' 3,95, 3,1 , 151,5 – – 46,2 0,08 – 2,4 5,2 – – ø 220,9 ' 0,0 0,0 4.503,9 646,0 56,2 2.676,0 XNUMX XNUMX XNUMX XNUMX XNUMX XNUMX, XNUMX XNUMX XNUMX XNUMX XNUMX XNUMX XNUMX XNUMX XNUMX ti
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TABLE NO. IV
Chemical analyzes of the main spring captures V-1 and V-3 from 1975 1976
June 1975 V-1 mg/1 V-3 mg/1 July V-1 mg/1 V-3 mg/1 August V-1 mg/1 V-3 mg/1 24.6.1975/10.6.75/28.7.1975 2.7.1975/19.8.1975/19.8.1975 19/2/36,58 32,83 .2 34,04/34,26/2 37,69/34,66/2 102,2g106,21+2 108,2 Mg106,2+ 2 104,2 Mg108,2+ 159,75 159,7 159,75+ Ca 156,2 163,3 Ca151,2+ 3 3.258 Ca3.221,75+ 03 3.246,16 Cl- 3.209,54 03 Cl- 3.221,75 3.256,15 Cl- 2 2.164 – – – HCO2.207 02 2.165 HC 2.248 2 2.327 HC 2.239,6 1 1, 3 CO1 free 1 1 C3 free 1 1 CO1 free 3 1 September V-16.9.1975 mg/16.9.1975 V-14.10.75 mg/30.10.75 October V-4.11.1975 mg/11.11.75 V-2 mg/37,69 November V-38,30 mg/2 V- 36,48 mg/42,96 14 2 34,04 38,9 2 Mg110,22+ 109,21 2 lig110,22+ 112,24 2 118,24g114,2+ 166,85 186,6 Ca172,17+ 168,18 175,72 ,191,7 Ca3t 3.209,54 3.185 Ca31,319,38. 03 3.333,78 Cl- 3 3.392,6 Cl- 3.394,8 2 Cl- 2.406,0 2.367 HCO2 2.411 2.371,6 He 2 2.525 – 2.371,6 – HCO1 1 3 .1 CO8.12.1975 free 8.12.1975 1 CO2 free 36,48 42,56 CO2 free 86,17 116,23 December V-124,2 mg/170,4 V-3 mg/2.562,7 3.270,5/2/2.147,0 2.160,0/XNUMX/XNUMX XNUMX;XNUMX+ XNUMX XNUMX CaXNUMX+ XNUMX .XNUMX XNUMX Cl- XNUMX XNUMX . HCOXNUMX XNUMX XNUMX COXNUMX free XNUMX XNUMX
Ó
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.
Continuation of table IV
January V-1 mg/l November V-6 mg/1 March V-1 mg/1 Mg1+ Ca2+ Cl- H2- CO003 free • 2 6.1.76 42,56 114,23 173,95 3.282,76 2.138 27.1.75 .43,17 117,24 175,73 3.319,38 2.226 Fe2+ Mg 2. Ca2+ Cl- HC 03 CO2-free 4.2.76 26.2.76 1,87 33,43 32,83 117,23 116,23 170,4 172,18 3.319,38 .3.319,18 2.279,2 2.164,8 2 mg2+ Cit3. Cl- HCO2- CO2.3.76free 30.3.76 38,1 38,91 119,24 110,22 172,18 175,73 3.331,58 3.331,78 2.059,2 2.182,4 1 April V-1 mg/1 May V -1 mg/1 June V-1 mg/2 2+ DKCa3+ Cl- – HCO2 CO6.4.76 free 14 14,78 112,24 181,05 3.319,3 2.374 27.4.76 35,73 113,23 173,95 3.343,54 2.279,2 2 i Mg2+ Ca3+ Cl- – HCO2 CO11.5.76free j 27.5.76 34,66 36,48 115,23 ; 114,23 175,73 179,23 3.368,19 3.368,19 2.277 2.204 2 2+ Kg Ca 11003. Cl- – 2 CO1.6.76free 8.6.76 38,3 37,08 113,23 117,23 181,05 181,05 .3.380,31 3.368,19 2.255 2.279,2 XNUMX XNUMX
June
V-1 eg/2.
Mg2+ Ca2+ Cl-HCO3- CO2 free 22.6.76/36,48/114,23 175,73 3.392,6 2.309 XNUMX XNUMX
VIII. NEW SOURCES OF MINERAL WATER
Throughout almost the entire history of spa operation, spa operators have tried to increase the yield and mineralization of the spring. All these efforts have been described in a historical overview. From more recent opinions and attempts, we extract: E. Wollmann was of the opinion in 1941 that it would be sufficient to conduct new tunnels. O. Hynie and K. Zima (1950), on the other hand, propose to first conduct 2 trial wells, outside the existing catchment area (both on the left bank of the river) in order to capture the tectonic direction E – W. In addition, they propose to conduct 2 exploratory hori -zonal core drilling across the fault system, from the bottom of the main pit to a distance of approx. 50 m in the northwest and southwest directions. Only after the execution of these wells will it be possible to better study the issue of the spring regime.
In 1963, G. Kačura solved the spring problem in Bílina with the help of three wells. Wells V 1, V 2 and V 3 were located in places where acid was mined in the past. They are located NE of the main pit (approx. 60 m).
Borehole V1 is an inclined core borehole (terrain elevation 222 m above sea level). Initial diameter 245 mm, final 137 mm. Depth 128,5 m. Definitive equipment: stainless steel casing 4 159/149 mm, solid to a depth of 39,5 mm, perforated to a depth of 64 m, 459/49 perforated from 64 to 128,5 m. Perforation 134 holes 8 mm .
Liquidation of the main spring shaft
After the connection of the new wells V1 – V3 to the receiving system of the spa and springs, all the springs in the main spring shaft gradually disappeared. It was therefore decided to dispose of this shaft.
Liquidation work took place in 1970-1971.
In the first stage (1970), Geotest Brno performed injection of wells with a clay-cement mixture on the lowest floor of the shaft. Later, a clay layer of several meters was proposed, which was covered with a concrete slab. On the upper floor in the place of the side studs in the main approx. 23 m, a steel casing O 221 mm was installed, brought up to above the terrain. This casing was sprinkled with duckweed in such a way as to allow the inflow of water from the tunnel and to serve as an observation probe. In II. stage (1971), the spring shaft was driven up to the surface with mostly clayey material from the Maxim Gorkij mine.
The observation probe is currently unmeasurable, probably clogged with clayey sediment. It will need to be cleaned.
IX PROTECTION OF THE SOURCE AGAINST UNDESIRABLE INTERVENTIONS
All data in this chapter are from the archive of the Czech Inspectorate of Spas and Springs of the Ministry of Health.
1) The main conflict of interests in the studied area could be the mining activity in the Mostek lignite basin. Therefore, one of the other goals of the hydrogeological survey should be sought in the protection of the Bílina mineral water from possible influence by mining.
All inspections to date at the mines of the lignite basin have not found anything objectionable in relation to the Bílina mineral water, even during mine water leaks in the 20s (Amelie III mine 1925; Venus mine 1928). It is clear from archive data that, for example, in 1928, 770 l/min of water flowed out of the Venus mine in Konobržl, and an average of 115 l/min of water was pumped out of the Svoboda mine in Braňany.
At the same time, both mine works are just behind or directly in the temporary protection zone of Bílinská kyselka. Other blowouts were recorded at the Minerva and Julius III mines. in Kopice (1943). However, there were even more smaller breakthroughs that were not caught by the mining inspection. The fact remains, however, that in Bílina none of the blowouts or deeper mine interventions had any effect.
Due to the protection of the Bílina spring, it was necessary to prevent any interference with the crystalline or basalt bedrock of the seams. Despite these facts, increased attention will need to be paid to this issue when delineating new protective zones.
Another unfavorable factor for mineral water could be the digging of drinking water wells. For the village of Braňany, soundings were carried out in 1909, 1911, 1923 and 1943. In addition, shallow wells and boreholes (approx. up to 8 m) were carried out at the northern foot of Kaňkovo. Even these interventions did not threaten the spring due to its small depth. Deeper wells, on the other hand, could endanger the mineral water regime.
So, for example, a 140,7 m deep well was drilled for Braňany, which found acid at a depth of 138 m and therefore had to be sealed. However, all these works were beyond the boundaries of the then protection zone. Among the other works carried out inside the protection zone, I mention sounding works for the village of Kaňkov, max. 9 m deep, wells for the village of Břežánky, two boreholes (85 m
deep) in Dlouhé djezd, excavated only in tertiary rocks, etc.
The city of Bílina was also forced to provide new sources due to the lack of drinking water. These actions were carried out (except for the current post-war ones) in 1854, 1889, 1911, 1923, 1930, 1939, 1940, 1943 and 1944. None of these actions threatened the spa's mineral water regime.
In 1930, 5 probes were excavated in Bílín to a depth of 8 m to obtain drinking water. These probes found the gneiss bedrock, but due to a complete lack of water, they were discarded. In 1943, 15 m deep boreholes were drilled in the Pagner (Ignis) mine field. Gneiss bedrock was not encountered.
Drinking water wells in the Žižka valley in Bílina /1953/ were also negative. In addition to these works, a number of wells were also made in Bílina, which did not catch acid.
Since 1907, gravel has been mined from the quarry on Želenické Hill. Because the businessman used large charges to blast rocks, the spa administration filed a protest, in which it mentioned
about the possible connection of these blastings with the decrease in the yield of the springs. However, blasting was carried out until the end of quarry operations.
Finally, an important factor for the potential impact of Bílina mineral waters is their contamination by irresponsible interventions, both natural and artificial. In 1966 (IV), for example, the City, NV in Bílina made an embankment from demolition buildings, while this action was not discussed in advance and its completion could threaten the bacteriological safety of medicinal sources. The event was halted and during April and May 1966 a protective measure was discussed to eliminate the defects.
In addition to the general disturbance of the appearance of the territory, roads, etc. the ČSD culvert was also disrupted, making it impossible to drain surface water, which could cause contamination. During the negotiations on the inspection of the landfill of demolition material, the spa organization did not agree with the landfill of unwanted objects, mainly in the immediate vicinity of the Bílina river.
During the construction of the railway track, the sewage system from Středočeské zřídel was broken. The representative of the ČSD undertook to ensure the construction of the proposed sedimentation pit, so that it would be possible to drain the waste water into the existing sewage system.
Despite the promise of ČSD representatives that the sewage and faeces from the local ČSD station will be taken directly to the public sewer - they are discharged freely into surface waters and already penetrate into the basements of the spa buildings, from where they have to be pumped out. Measures have been taken to eliminate this serious hygiene defect. A series of negotiations between the spa and the implementing company
(Construction Geology) concerned the modification (regulation) of the Bílina River. The management of the spa enforced the conditions to prevent any mineral water from coming into contact. In the event that the layer with CO2 is hit or the groundwater is contaminated with phenol, it is necessary to load the damaged area with clay material in order to restore normal conditions.
The improvement of the river was planned in the route between the town of Bílina and the railway bridge near České Zlatník (7 km). 59 drilled and dug probes with a maximum depth of 7,50 m were excavated. Despite all the mentioned examples of possible contamination near the spa, the collected water was still bacteriologically harmless, which testifies to the perfect design of the wells.
However, this problem, despite the stated finding, needs to be given due attention.
X. PROTECTIVE ZONE
The first original protective district was approved by decree of the former spa governorship in Prague dated 5.10.1872 under reference no. 567. It was established on the basis of the good appearance developed by Professor AE Reuss. The proponent justified its relatively small area by the favorable geographical and geological conditions in the vicinity of the spa.
The developing mining activity (lignite mines) beyond the western border of the zone forced its enlargement in 1889. The welcome was compiled by professors G. Laube and Fr. Steiner. This extended protection zone, which was in effect 20 years ago, was approved by a decree of the mining governorship in Prague on 18.4.1891 April 516 under reference no. XNUMX.
Provisional Protection Zone (1955)
In 1955, K. Zima examined the existing protective area and concluded, quite correctly, that it unnecessarily occupies the right-bank Bílina area (Liběšice – Bořeň – Skalka) and the area of the southwestern slope of Kaňkovo, while on the western border (the western slope of Mnichovce), the western vicinity of the Amelie III mine ( north of the FUgner mine) the protective zone occupies an area that is too small. Here he designed a protective
extend the zone to the edge of the Tertiary basin. In his opinion, the mining of lignite seams does not threaten mineral water, because there is a sufficiently thick layer of clay in the bedrock of the bedrock, which separates the bedrock from the crystalline bedrock.
However, the proposal for protective belts from 1955 by K. Zima was not announced, and therefore not approved as provisional. Nevertheless, I present the definition and situation of the narrower and wider protection zone for their logical justification (appendices 12 and 13).
a) A narrower protection zone must be defined, because it is necessary to ensure the provision of hygienic and spring technical conditions inside the spring area, excluding the effects of adverse interventions in the shallow water regime.
It is assumed that all earthworks, trial sounding and digging of private and public wells will be prohibited. Earthworks do not mean shallow furrows up to a depth of 1,0 m and overburden during terrain improvements aimed at improving conditions, such as park improvements, excavations for protective walls and excavations for installation lines and electric poles, etc.
A narrower zone that would secure the spring area and compliance with the above-mentioned measures is summarized by K. Zima as follows (situation 1 : 2).
"Starting point A is south of the swimming pool across the river at cat. border of Bílina, the strip line crosses the river to point B (joint of land no. 810, 811, 812 and 813)•runs to C (SZ cat. no. 809) to D (joint no. 908 and 809) according to border 908 to E (junction no. 910 and 911) then to F (no. 602/2 and 601/1) further on G and H according to the boundary of the land no. 601/1 from where in a straight line to point J (junction no. 600 and 559 on the NE tip no. 599 – to point K (junction no. 506, 612 – 504, 503 and 613) from there to L on bend of the Bílina city cadastre at the starting point no A.
b) a wider protective zone is intended to protect the spring from deeper artificial interventions in the bedrock of gneisses and basalts, which represent the environment for the formation of mineral waters and, together with the tectonics of the area, are the main indicators for its delineation. The extent of the band also takes into account the geographically visible infiltration area, which determines the circulation of vadose fracture waters of deeper zones, where
to the gasification of incoming CO2 and to directional tectonics, represented by the Bílin fault and accompanying faults.
The protection zone does not cover the Svoboda mine field (situation 1 : 8); in this direction it will be necessary to expand it,
The sealing packer is located at a depth of 39,00 — 39,50 m; the annulus above it is filled with a clay-cement mixture.
Groundwater with the character of Bílinská kyselka was found at a depth of 42 – 43 m in a more heavily disturbed zone. The output was 30 – 40 1/min.
Well V – 2 is an inclined core well (terrain profile 229 ni nm). Initial diameter 267 mm, final 98 mm. Depth 243,3 m. Definitive equipment: pin casing and anti-corrosion steel 6 159/149 mm to a depth of 57,7 m. Perforated casing 6 59/49, from 55 m to 183,3 m (found). Perforation 13%, 6 8 mm. Sealing packer at a depth of 55 m, the annulus above it is filled with a clay-cement mixture. According to resistivity measurements, there are uniform inflows into the well along the entire length of its walls and its bottom.
Borehole V 3 is a vertical wide-profile borehole dug to 64 m with an impact depth of 6 mm. A core was drilled to a final depth of 475 m. Final profile 130 mmm. Definitive equipment: stainless steel booms 220 6/159 mm up to 149 m, perforated up to 40 m. Wooden perforated booms 57 6/118 mm from 100 m to 55 m. Perforation 130%, at a depth of 13 m there is a sealing packer , above it a clay-cement seal up to the ground. Under the packer is a stabilizing cover. The main tributaries detected by resistivity measurement were at depths of 38,8 m, 78 m and 82 m. With regard to the protection of water resources, a maximum withdrawal of 88 3/min was allowed from V laz V 28,8. with a current consumption of 1 7/min. on V1.
If the sampling criteria are respected, the amount of CO2 will be between 1900 - 2200 mg/l, the alkalinity will be between 71 - 73 mval/1 and the water level will be above 190 m above sea level
Any ill-advised increase in extraction carries with it the risk of breaking the complex hydraulic and hydrochemical balance of the resource, associated with the subsidence of the water level and the loss of CO2 content. The wells capturing the acid lake on its way out show a 5x higher yield of mineral water compared to the earlier collection.
G. Kačura explains the genesis of kyselky as follows: The formation of kyselky occurs in gneiss by the action of water with dissolved CO2 on aluminosilicate systems. The output of CO2 (whose origin may not be juvenile) is conditioned tectonically. Currently, water from V1 is used for foaming and mineral water from V3 for baths. Water from V 2 is not yet used for increased Pe content. According to the guidelines for the operation, maintenance, measurement and extraction of mineral water from new wells, the groundwater level at V 1 should optimally be lowered to the level of 36,22 m, from the edge of the casing, while the yield (free outflow in front of the spring vase) should be approx. 20 1 / min. With this adjustment of the pump, the excess pressure b:jt should not be greater than 0,5 - 0,6 kp. At the same time, G. Kačura considers 34 1/min as the maximum possible limit of withdrawal from new wells. (for the dressing room 28 1/min and for baths 7 1/min.). In the second used well V – 3, according to the guidelines, the water level should be lowered to the level of 33,97 m from the edge of the casing with a yield in front of the spring vase of 10 1/min. Overpressure on the wellbore in the spring weight should not be more than 0,4 - 0,5 kp.
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In the attachment, the old protection area is drawn in yellow. The new wider protection area is given its course as follows:
The starting point "a" is at the contact of č.k. 320 and 319 in the cadastral territory of the municipality of Břežánky, from there the line runs identically to the old protective zone up to point "b" on the no. 1088 (Bílina cadastre), then to "c" on the Újezd cadastral border, along it to point "d", then in a straight line to "e" at the intersection of cat. territory of Újezd, Chouč and Liběšice, to point "f" at the intersection of the cadastral border between Liběěice and Želenice and the road at the intersection of cat. border between Liběěice and Želenice and the road to Želenice, from there along the southern edge to "g", from there to "h" (eastern corner of č.k. 1445 želenice), then to "ch" according to č.k. 1447 and 1694 to contact no. to. 1702 and along 1702 on "j" lying not on the line of the old protection zone and along this border to point "k" on č.k. 151 Braňany. From there, an extended protection zone is proposed to point "1" at the tip of the cadastre, the border to the starting point "a".
The author does not consider the extension of a wider protective zone against mine fields with a lignite seam to be necessary. However, it cannot be accepted that the crystalline substratum of the sedimentary Tertiary series of the Mostek basin is eroded. Otherwise, after evaluation, the wells must be concreted, the exposed bedrock must be immediately isolated from the surface, and any seeps must be sealed. All hydrological and geological findings must be reported to the Inspectorate of Spas and Springs. In addition, it is necessary to carry out regular mining trips and to submit reports on the progress of work to the Czech Inspectorate of Spas and Springs to keep records on the progress of felled fields.
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Provisional protection zone (1960) Pursuant to Government Resolution 1030 of 1958 and respecting the directive of the Ministry of Health, a proposal for temporary sanitary protection zones for the spring in Bílina was submitted in 1960, which was prepared by G. Kačura and V. Myslil. In the following text, I present the basic findings of the proposal. the wider area of Bílina - today's mineral water catchment - lies at the edge of the Tertiary basin Mostecko - Duchcoveko - Teplické and on the edge of the volcanic area of the Český středohoří. The deepest subsoil consists of gneiss, which is partially and irregularly kaolinized. On it, Upper Cretaceous sediments are deposited in the development of sandy marls or marls with limestone positions. They are discordantly overlain by sediments of Tertiary age, mainly Miocene. They are underlying clays on which a layered zone rests, which in most areas is covered by overlying clays. Pliocene and Pleistocene gravels are preserved in rare relics. Tertiary volcanics are represented here by cherts, basalts and tuffites with their tuffs and tuffites. Slope valleys are covered with thick rubble and rubble clay. Loess approaches them inside the basin. The earth (mainly in the basin) is strongly influenced by mining activity (quarries, shafts, collapses, famines). Tectonic structure is manifested in the basin and outside the basin. Several studies can be distinguished, of which the older ones mainly affect the structure of crystalline and chalk (the younger one is significantly manifested by the violation of Tertiary sediments (coal seams).
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The fractures have two distinct directions. Ore Mountains -longitudinal and associated transverse - radial. Apart from these breaks, it is possible to infer the direction of the Jizera from the entire structure.
The mineral springs of the Bílina spa are tied to cracks in the gneiss (NW-SE direction). Determining the regularity of the circulation is not quite possible in the given case, because some even more open fissures can be sealed in certain parts, either by products of ventilation of the rock itself or by plugging with secondary displaced materials of weathering processes. The output of carbon dioxide and the gasification of the rock are not limited only to the place where today's mineral water is captured. Carbon dioxide was also detected, for example, at the interface between crystalline and chalk in Brariany (in 1940). Gasification was further detected in the coal seam at the A. Jirásek mine in 1959. The mineral water in Bílina belongs to the acid sodium-bicarbonate type with an increased content of 0a2+, kg2+, SO42- and Cl- due to its chemistry. The waters circulating in the fissures of the crystallinics are also of the same type. Taking these geological and hydro-geological conditions into account, in 1960 the narrower protection zone was limited to the immediate vicinity of the catchment area. The protective zone defined in this way was considered by the already and newly conducted research into the acid bath regime (i.e. using new wells to supply the baths). a wider temporary protection zone was extended against the valid protection zone from 1891 due to the geological and hydrogeological conditions mentioned above, especially to the northwest to the Braňany cadastre and to
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northeast, where it follows on from the wider temporary protection zone of the Teplice Spa from 1959. In the wider temporary protection zone, due to the fact that the occurrence of acid is linked to the crystalline subsoil, the mining of coal or underlying clays is not restricted, unless of course these clays do not sit directly on crystalline material.
Protection zones are listed in Appendix No. 14.
XI. HYDROGEOLOGICAL SURVEY DRAFT
The hydrogeological works of the 2nd and 3rd phases will be specified in more detail in the concept and implementation project, which will be submitted in the 2nd quarter of 1977. The Bílinská area is moderately geologically and hydrogeologically explored. Among the older authors, G. Laube (1898) and JE Hibsch (1924) gave a detailed geological description, the latest geological information can be found in the explanatory notes to the Teplice 1 : 200 sheet by V. Zoubek and J. Škvor from 000. About the immediate surroundings of the springs mineral water is mentioned in the explanatory notes of the Teplice 1963: 1 P. Macák et al. in 50.
The most important hydrogeological research comes from K. Zima and O. Hynia (1950, 1953, 1955), the most recent hydrogeological research was carried out in 1959-1965 by Georgij Kačura and published in 1967.
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3) Laboratory work In addition to the laboratory analyses, mentioned in the "regime observation" section, I recommend carrying out a new bacteriological research. Sources of drinking water from the immediate vicinity of the spa should also be bacteriologically examined. From the point of view of the protection of the Bílina spring, it will be appropriate to carry out analyzes of the surface water•from the Bílina (Bělé) river, mainly from the part of the flow above the mineral water sources. It can be assumed that specific polluters will be detected.
xii. i live
The preparation of the research study as the first phase of the hydro-geological survey for the determination of protective zones was based on the study and extraction of available archive materials from the relevant archive fund of the Ministry of Health and in the Prague Geofund. Several graphic materials were lent by the Directorate of Central Bohemian Springs in Bílina. The submitted research report ee consists of eleven basic chapters. After the introduction, in II. chapter a chronological list of the authors and their work on the Bílin spring from 1788 to 1967. III. In a historical overview, the chapter deals with mineral springs, their occurrence, remedial works and reconstructions, and the development of their extraction from their discovery to the present day.
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Even before the definitive protective measures are established
it will be necessary to carry out some survey work in the belt,
of which I recommend:
1) Mode observation
a) Climatic factors: average daily temperature, daily
total atmospheric precipitation and barometric pressure
(once, daily).
b) Hydraulic parameters: levels, yield (1 of
daily) in the assumed I. protective zone iu
more important sources of plain groundwater.
c) Water chemistry parameters: abbreviated chemical analyses
for all used and unused mineral
springs 1 x a week.
',piny chemical analysis of all mineral springs
1 x per month.
d) In addition, the water temperature should be measured
for all mineral springs and selected sources
plain groundwater in the vicinity of the spring.
2) Drilling and collecting work:
To specify the genesis of mineral waters and possible
I recommend increasing the overall yield of mineral springs
continue to carry out further drilling work in the area to the west, south
west and northwest of existing water sources,
where further occurrence of mineral water can be expected.
I do not consider it necessary to carry out additional geophysical
work or tracking tests, given that the evaluation
valuing these works would be quite problematic.
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IV. the chapter is focused on geology and tecto-
niche in connection with the creation of mineral water.
V. The chapter deals with hydrogeological conditions
area.
VI. the chapter is dedicated to Bílina mineral water –
– its chemical and physical properties and that with respect
on the therapeutic effects of the medicinal source.
VII. the chapter deals with the hydrochemical properties of
carry the spring. This part of the report is completed by four
tables with chemical data from older and more recent ones
archival materials.
In VIII. chapter summarizes information about new
sources from 1959-1965.
IX chapter provides information on protection
sources from unwanted interventions. The main ones are described here
mining interventions (drilling and kicking work) in the wider protective
band.
They are described chronologically in Chapter X
all temporary protection zones, including K. Zima's proposal
from which the authors of the current provisional bands were based
XI. the chapter is then devoted to some proposals
for the 2nd phase of the hydrogeological survey (regime measurement,
drilling work, laboratory work, etc.).
2nd phase of search survey for determination
definitive protective belts of the spa Bílina, will bring
additional knowledge about the spring structure of Bílinská kyselka
and the basis for its definitive protection and stabilization
regime.
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LITERATURE
1) GINTL W. – LAUBE U. STEINER F. (1898) : Die Mineral-
wasserquellen von Bílin in B3hmen und die
an denselben in den Jahren 1888 – 1890
durchgefUhrten Sanie rungsarbeiten,
Bílina
2) HIBSCH JE (1924): Erlguterungen zur geologischen
Map of the environment of Bílina, Prague
3) HYNIE 0. (1963): Hydrogeology of the Czechoslovakia II. Mineral
vody, 448 – 452 Prague
4) HYNIE 0. – ZIMA K. (1950): General geological survey
about mineral springs in Bílina. Archives
Ministry of Health, Prague
5) KAČURA G. (1963): Second report on regime research
kiselky in Bílina. Report geol. test
in 1962 Prague
6) KAČURA G. (1966): Hydrogeological solution of the structure
Kyselky spring in Bílina. – Geotest Prague
7) KAČURA G. (1967): Spring structure of the Bílina Kyselka.
SG. geol. sciences, ř. HIG, Vol. 5 Prague
8) KAČURA G. – MYSLIL V. (1959): Design of protective belts
Kyselky in Bílina. – Geofund Prague
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9) KISCH EH (1879): Die Heilquelle und Curorte
B6hmens in historischer topographischer,
physikal-chemischer und medicischer
Hinsicht – Braumillers Bade – Bibliothek,
93. Vienna
10) LAUBE GC (1884): Geologische Exkursionen im Thermal-
gebiete des nordwestlichen amen*.
Leipzig
11) LOSCHNER J. (1859): Der Sauerbrunn zu Bilin. Prague
12) PIŠTORA Z. (1963): Final report on the execution of the reservoir
wells (sources of drinking water) in Bílina. –
Geofund Prague
13) REUSS AE (1845): Der Sauerbrunn zu Bilin in
Bohemian Prague
14) REUSS PA (1788): Naturgeschichte der Bilin Sauerbrun-
nen in B3hmen, Prague
15) THEIMER K. (1891): Quellenweiterung am Biliner
Sauerbrunn Erzgebirgs – Zeitung,.
Year 12, Teplice
16) THEIMER K. (1892) : (ieschichtliches öber den
Swerbrunn bei Bilin. – Erzgerirgs –
Newspaper
17) VRBA J. (1955): Evaluation of hydrological observations
at the mineral springs in Bílina in years
1941 – 1946. Archive of the Ministry
healthcare. Prague
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18) WOLLMANN E. (1942): Gutachten ilber das Bad und den
Heilwasser versandbetrieb Bilin und den
Heilwasser – versandbetrieb. Archives
Ministry of Health Prague
19) ZIMA K. (1953): Hydrogeological conditions in the vicinity of Bílina.
Archives of the Ministry of Health Prague
20) ZIMA K. (1955): Mineral geology and balneohydrology
source in Bílina in Bohemia. Archive of the Ministry
healthcare. Prague
21) ZOUBEK V. – ŠKVOR V. (1963): Explanations for the clear
geological map of Czechoslovakia 1:200, sheet
Teplice and Chabařovice. Prague
Prague, March 1977
Prepared by: Pg. Vl. Cyvin
Head of department: RNDr. Laboutka
RNDr. Jaroslav /11;2W1č Pg. Stanislav at 1 a
head of the hydrogeological area geological nšmětk