GROUND UPLIFT AFTER THE CLOSURE OF WATER LEAKS IN THE MINA DRIFT OF THE WIELICZKA SALT MINE

Geology, Geophysics & Environment 212 Vol. 38 No. 1 9 22 http://dx.doi.org/1.7494/geol.212.38.1.9 GROUND UPLIFT AFTER THE CLOSURE OF WATER LEAKS IN THE MINA DRIFT OF THE WIELICZKA SALT MINE Wypi trzenia terenu po zamkni ciu wycieku w poprzeczni Mina w Kopalni Soli Wieliczka Agnieszka Maj 1, Grzegorz Kortas 1 & Pawe Ulmaniec 2 1 Instytut Mechaniki Górotworu PAN; ul. Reymonta 27a, 3-59 Kraków; e-mail: maj@img-pan.krakow.pl 2 Kopalnia Soli Wieliczka SA; Park Kingi 1, 32-2 Wieliczka; e-mail: pawel.ulmaniec@kopalnia.pl Abstract: After putting the water leaks in the Wieliczka Salt Mine under control, upon construction of dams in 27, the ground subsidence stopped. Presently, however, ground uplifts are observed on land surface. This paper presents geological, mining, and hydro-geological conditions occurring in the leak areas. Using the examples of previous subsidence, the authors have demonstrated the shaping of ground uplifts observed in levelling surveying by precise measurement methods. With a correction relating to the subsidence caused by working convergence that also occur in ground displacements, it was found that the maximum ground uplifts reached 63 mm, with the continuing trends in the years to come. It was established that the causes of uplifting included increase of pressure in suffosion caverns and the displacement effect, with irrigation of dried and drained formations during the ow of water into the salt mine. Key words: Wieliczka Salt Mine, subsidence trough, ground uplift Tre : Po opanowanym wdarciu wód do Kopalni Soli Wieliczka przez zamkni cie wycieku w 27 r. usta y obni enia powierzchni i obecnie wykszta caj si wypi trzenia. W pracy przedstawiono warunki geologiczno-górnicze i hydrogeologiczne w stre e wycieku i na tle poprzednich obni e pokazano kszta towanie si wypi trze terenu, obserwowane w pomiarach geodezyjnych niwelacj precyzyjn. Bior c pod uwag poprawk na uczestnicz ce w przemieszczeniach terenu osiadania spowodowane wp ywami kopalni, stwierdzono, e maksymalne wypi trzenia osi gn y 63 mm, a teren w nast pnych latach mo e si nadal wypi trza. Wskazano, e przyczyn wypi trze jest zwi kszenie ci nienia w kawernach sufozyjnych oraz efekt wyporno ciowy i nawadnianie osuszonych i zdrenowanych utworów w trakcie sp ywu wód do kopalni. S owa kluczowe: Kopalnia Soli Wieliczka, niecka osiada, wypi trzenia terenu

1 A. Maj, G. Kortas & P. Ulmaniec INTRODUCTION Water penetration into the Mina drift at Level IV of the Wieliczka Salt Mine in 1992 caused the occurrence of considerable deformations on the northern Salt Mine foreground. Leak containment and rock mass sealing allowed to put the water hazard under control and leak plugging in 27. The circumstances and the course of water penetration, with its characteristics, evaluation, and threat analysis, were the objects of a number of studies and publications (e.g. Garlicki & Wilk 1993, Studium 1995, Bromowicz & Brudnik 1997, Gonet et al. 1997). in this paper, we present the geological and mining conditions of the water leak area, discussed in detail in many papers (e.g. Garlicki & Szybist 1995, Na cki 1995, Kortas 24, d Obyrn & Przyby o 21). Based on the results of the measurements of subsidence at the stage of leak activity, we have discussed the observed displacements that were typical for the process of natural hydro-geological condition recovery. GEOLOGICAL AND MINING CONDITIONS The geological structure of the border zone of the Wieliczka rock salt deposits is quite complex. The zone width is changing from 2 m to 5 m. A gypsum cap is adjacent to the deposit, with distant Skawina formations, mixed with Carpathian ysch and Chodenice sandstone formations. Such formations are often torn apart and they overlap in the form of crests or scales. Sandstone blocks have the dimension of ca. 2 m, and their accumulation is chaotic. They are shifted apart, locally separated by silt formations, and they create crevices and caverns. Finegrain, compacted or loose, and even disintegrating sandstones show the traces of karst activities and water ow. Locally, we can nd within sands some fragments of the crushed gypsum cap. That zone is a path of water links of several water subsystems (Garlicki & Wilk 1993). The Mina drift cuts the deposit boundary at the horizon of 76 m a.s.l. Its northern edge overcomes the gypsum cap and opens a water link with the water contained in the Chodenice sandstone layers. The deposit structure in that area and the location of the Mina are characterized by the geological cross-section presented in gure 1. The rock mass and land surface deformations have been shaped by primary and secondary geological conditions occurring in the Chodenice layers since the time of water penetration. Those formations isolate the deposit from the contacts with Quaternary and surface waters. Fine-grain, silted and dusty sandstones occurring there, with diverse ltration coef- cients from 1 1 m/s to 1 6 m/s, create aquiferous layers, allowing for water ows within the space between the boulders of crushed sandstones (Garlicki & Wilk 1993). As a result zof tectonic disturbances and karst processes around the Mina drift, local systems of water circulation were created within two or three sandstone stratiforms. The area around the Mina drift is the northern part of the central Salt Mine area. Under the Mina, there are 19th and 2th century dry extraction chambers and about a dozen of 2th century leached caverns. On the top levels, there are some chambers and gallery workings. Such workings are subjected to volumetric convergence at small rates of up to 7.3 /year, and locally even 11.1 /year. The chambers situated on Levels IV to VIII were back lled, but convergence will stop only after the back ll obtains adequate support strength.

Ground uplift after closure of water leaks in the Mina drift of the Wieliczka Salt Mine 11 Fig. 1. Geological cross-section of the Mina drift (Ulmaniec 24, after: Brudnik & Szybist 1995) Fig. 1. Przekrój geologiczny przez rejon poprzeczni Mina (Ulmaniec 24, za: Brudnik & Szybist 1995) The breach of the deposit boundary in the Mina drift in 1912 caused the appearance of a leak, and 226, m 3 of water penetrated by 1992. With the average leaching density of 4 g/dm 3 NaCl, water entered the surface area of ca. 4,2 m 3. Water penetration that occurred in 1992 initiated a number of rapid ows which changed into an almost uniform leak with decreasing yield (12 dm 3 /min before plugging). A long-term drainage of aquiferous formations caused the out ow of 45, m 3 of insoluble parts and NaCl together with water. The washed rock material plugged suffosion canals, while increased water pressure made them wider. Periodic high hydraulic gradients were the cause of the suffosion processes. Periodic subsidence, with ground uplift when the leak decreased within the suffosion trough, became secondary symptoms of that process. Plugging of the leak in 27 started the process of reinstatement of natural hydrogeological conditions: water table increase with void lling, watering of drained formations, and rebuilding of natural pressures. The in uence of those processes on the ground movements have been still observed.

12 A. Maj, G. Kortas & P. Ulmaniec GROUND DISPLACEMENTS AFTER LEAK PLUGGING IN THE MINA DRIFT The surveying measurements have been conducted on the northern foreground of the salt deposit since the 192 s. A dense network of observations of the uncontrolled water ow effects was established after the intense leak of 1992. in the subsequent months, the maximum ground subsidence (Benchmark S-5 and later S-3) reached 14 cm/day. Recent rapid ground displacements occurred by the end of April of 1993. Later, the ground subsided at different but slowing rates from 25 mm/year to 2 mm/year (Figs 2, 3), until the leak was plugged. Since 27, the ground was regularly lifting up, according to the precise surveying method measurements conducted by P. Ulmaniec (Fig. 3). -5 Vertical displacement w [mm] -1-15 -2 Benchmark s-5 (and later s-3) Benchmark P-5-25 Years of measurements 1992 1993 1994 1995 1996 1997 1998 1999 2 21 22 23 24 25 26 27 28 29 21 211 Fig. 2. Benchmark S-5 vertical displacement (Ulmaniec 24) Fig. 2. Przemieszczenie pionowe reperu S-5 (Ulmaniec 24) In the rst year after leak plugging, the maximum displacement of +21 mm was found at Benchmark S-26. The uplift area of more than 1 mm on the surface of ca. 6 hectares covered the deepest central and eastern parts of the suffosion trough. Maximum 29 uplifts were observed at Benchmarks S-27 and S-31: +33 mm. The +1 mm isoline of 27 29 covered nearly the whole area of subsidence of more than 1 mm identi ed in the observation period of 1992 27 (Fig. 4).

s-11 R-66 s-1 R-67 s-55 s-22 R-69 s-48 s-54g s-8 SK1 Rp938 s-7 s-245 s-46g R-51 R-138 s-24 s-52n s-19 R-139 s-213 s-6 s-243 s-31 s-212 s-45 s-255 s-227 s-18 s-242g s-51 Kl-2 R-13 R-129 R-129a s-211 s-248 s-254 R-128 s-226 s-241 s-217 Zn3 Zn6 s-44 s-3 s-21 s-3 R-45 R-123 R-127 s-253 R-13a s-225 s-5 s-17 s-24 R-44 s-247 R-43 R-122 R-12 R-121 s-138 R-131 R-113 s-1 s-4 s-224 s-31 s-239 R-42 R-115g R-116 R-114 s-32 s-43 s-29g D-12 s-21 s-238 R-39 s-99 R-16g s-27 s-246 R-4 s-232 s-222 s-3 s-237g s-28 s-26g R-15 s-63 s-221 D-9 R-14 s-15n s-18 R-13 R-12 s-231 s-62 s-23 s-25g Pp14 s-214 s-42n R-1 R-98 s-61 s-27 s-219 R-99 s-228 D-5 s-2 s-19 s-26 R-93 s-49 s-13 R-17 R-169 R-34 R-168 R-167 R-166 s-12g R-161 R-84 R-16 R-83 R-158 R-8 s-14 R-148 R-147 R-145 s-16 s-17 Ground uplift after closure of water leaks in the Mina drift of the Wieliczka Salt Mine 13 Vertical displacement w [mm] -227-228 -229-23 -231-232 -233-234 -235-236 -237-238 -239-24 -241-242 -243-244 -245-246 Years of measurements 1994 1995 1996 1997 1998 1999 2 21 22 23 24 25 26 27 28 29 21 211 212 15 1 5-5 -1-15 -2-25 -3 Vertical displacement rate dw/dt [mm/ r] Fig. 3. Benchmark S-5 vertical displacement and displacement rate since 1995 Fig. 3. Przemieszczenie pionowe reperu S-5 i pr dko przemieszczenia od 1995 r. 233 232 231 B-3 R-91 R-92 23 229 pop. Mina 228-86 -859-858 -857-856 -855-854 -853-852 Fig. 4. Distribution of uplifts after leak plugging in the Mina drift in 27 29, in mm Fig. 4. Rozk ad wypi trze po zamkni ciu wycieku w poprzeczni Mina w okresie 27 29, w milimetrach

14 A. Maj, G. Kortas & P. Ulmaniec By 21, the maximum uplifts occurred behind the railway line, 2 m north from the leak dam, and they reached the value of +49 mm. In total, the maximum uplifts after leak plugging by autumn of 211 amounted to +63 mm, with slight expansion of the +1 isoline (Fig. 5), and uplift volume of ca. 2,3 m 3. 233 s-14 s-18 s-16 s-11 s-22 R-123 R-122 s-19 s-17 232 231 23 s-1 s-8 s-48 s-55 R-66 R-67 s-54g R-69 SK1 Rp938 s-7 s-245 R-138 s-46g s-19 s-24 R-51 s-52n R-139 s-213 s-6 s-243 R-12 R-121 s-138 R-127 R-118 R-128Rp936 s-99 s-31 R-16g R-115g R-17 Kl-2 R-13 R-116 R-129 R-129a R-13a R-114 s-3r-131 R-113 s-227 s-1 s-212 s-45 s-51 s-18 s-226 s-211 s-242g s-255 s-217 s-225 s-21 s-3 s-241 s-17 s-24 s-31 s-4 s-239 s-29g B-3 s-32 s-34 s-21 s-43 s-238 s-232 s-222 s-27 s-3 s-246 s-28 s-63 s-26g s-237g R-14 R-15 R-13 R-12 s-15n D-9 s-62 s-231 s-23 s-25g Pp14 R-1 s-27 s-214 s-219 D-5 s-228 s-2 R-93 R-92 R-91 s-26 R-169R-168 R-17R-167 R-166 R-165 s-12g R-161 R-16 R-84 R-83 R-158 Rp336 R-8 R-148 R-147 R-145 s-5 229 pop. Mina Zn3 D-12R-4 R-43 R-42 R-39 R-45 Zn6R-44 s-42n s-49 228-86 -859-858 -857-856 -855-854 -853-852 Fig. 5. Distribution of uplifts after leak plugging in the Mina drift in 27 211, in mm Fig. 5. Rozk ad wypi trze po zamkni ciu wycieku w poprzeczni Mina w okresie 27 211, w milimetrach R-34 ANALYSIS OF GEODETIC GROUND MOVEMENT OBSERVATIONS The comparison of subsidence occurring before leak plugging and afterwards can be demonstrated on the example of several benchmarks placed in the trough centres in various periods. We observed change from subsidence to uplifts on all benchmarks, with more and more regular uplift rates (Fig. 6). The shaping of the uplift trough is illustrated with cross-sections. in the 1992 27 trough cross-sections were dominated by the effects of rapid and considerable subsidence caused by rock mass dehydration and suffosion of 1992 1993 (Fig. 7). In the rst year of uplift observation, the trough was shaping on both sides of the railway line, above the subsidence centre of the previous period and at the sandstone outcrop. in the subsequent years, the southern centre disappeared, and the maximum uplifts were found above the sandstones, with a typical trough elongation on the sandstone stretch.

Ground uplift after closure of water leaks in the Mina drift of the Wieliczka Salt Mine 15 B-3 s-31 s-3 s-241 s-34 s-15n s-27 s-26 Mina Vertical displacement w 23-211 [mm] 5 4 3 2 1-1 -2-3 -4-5 -6-7 s-248 s-31 s-34 s-3 s-241-8 Years of measurements -9 23 24 25 26 27 28 29 21 211 212 Fig. 6. Locations of benchmarks and cross-section lines, with vertical displacement of annual trough centres in 24 211 Fig. 6. Lokalizacja reperów i linii przekroju oraz przemieszczenia pionowe centrów rocznych niecek w latach 24 211

16 A. Maj, G. Kortas & P. Ulmaniec SE corner of the Monastery B-3 27-211 railway line 1995-27 dam in Mina 5-4 -8-12 -16-2 4 3 2 1 1 2 3 4 5 6 7 8 9 1 11 12 13 14 15 16 17 18 19 2 21 22 23 24 25 26 27 28 Subsidence 1992-27 [mm] 27-21 27-29 27-28 1992-27 Distance [m] Uplitf 27-211 [mm] Fig. 7. N-S subsidence trough pro les and uplifts shaping Fig. 7. Pro le N-S niecek obni e i kszta towanie si pro lu niecki wypi trze The observed vertical displacements are the total results of the uplift caused by rebuilding water table and land subsidence caused by the mine workings convergence. The constant rate of volumetric convergence is associated with the constant rates of land subsidence, also on the related surface. For that reason, the actual sizes of the uplifts caused by lling of the depression funnel by water are getting larger. We can infer from our observation of subsidence before water penetration into the Mina drift that the areas of the trough centre subsided with the range of ca. 4 mm/year. Assuming that similar subsidence results from the current in uence of the converging workings on the land surface, we can correct elevations of Benchmark S-241 and S-34 to +16 mm/4 years. The correction results are visible on the benchmark uplift graphs (Fig. 8) and the pro les of gure 9. Implementation of that correction leads to a change of the uplift distribution and increase of the uplifted mass volumes to V w = 2,6 m 3. The range of the uplift trough is enlarging towards the Mina drift, and the southern trough slope is getting milder (Fig. 9). The piezometric water level measurements taken in Borehole B-3 indicate that two separate rates of water level increase appeared during the depression funnel lling. Initially, after Pipe D-1 was removed, the rate was k 1 = 8 m/year. Later, after the damper was closed on Pipes D-2 and D-3, the rate decreased to k 2 = 3 m/year (Fig. 1). The range change was also re ected in benchmark uplifting. The volume of the original voids and those created during rock uplifting was estimated at V p = 11,5 m 3 (Kortas & Maj 211). Consequently, the proportion of the trough uplift volume to the void volume is V w /V p =.23. The uplifts caused by elastic mechanical reaction resulted from increasing pressure on void walls, proportionally to the height of the water level, as well as the displacement effect. Formation swelling, especially clay swelling caused by humidity was another reason of that process. in the rst year, the subsidence and uplift

Ground uplift after closure of water leaks in the Mina drift of the Wieliczka Salt Mine 17 centres were matching, and the effects of mechanical reaction were dominating uplift components. Positive volumetric convergence and upward directed vertical displacements developed in suffosion caverns. Later, the trough uplift centre moved north. That could have been caused by the lling of shallow voids situated in sandstone outcrops, although the duration of the process indicates that the results of previously drained and dried formation watering could be dominating. 7 6 Uplift w 27-211 [mm] 5 4 3 + 8 mm + 12 mm s-241 + 16 mm 2 1 + 4 mm Subsidence 1984-1992 4 mm/year Years of measurements 27 28 29 21 211 212 7 6 s-34 + 16 mm 5 Uplift w 27-211 [mm] 4 3 + 8 mm + 12 mm 2 1 + 4 mm Subsidence 1984-1992 4 mm/year Years of measurements 27 28 29 21 211 212 Fig. 8. Benchmark S-241 and S-34 uplifts after accounting for the workings uplift in uence on the surface Fig. 8. Wypi trzenie reperów S-241 i S-34 po uwzgl dnieniu wp ywów na powierzchni terenu zaciskania wyrobisk

2 4 6 8 1 12 14 16 18 2 22 24 26 28 18 A. Maj, G. Kortas & P. Ulmaniec SE corner of the Monastery B-3 railway line dam in Mina 12-1 11-2 1 Subsidence [mm] -3-4 -5-6 -7-8 -9-1 Real uplift 27-211 4 years Measured uplift 27-211 4 years Estimated subsidence by 1992 4 years 9 8 7 6 5 4 3 2 Uplift [mm] -11-12 Distance [m] 1 Fig. 9. Imposition of the land subsidence and uplifting processes Fig. 9. Nak adanie si procesów osiadania wypi trzania terenu Depth of water table H B-3 in B-3 [m] 1 2 3 4 5 6 7 8 9 1 11 12 13 14 15 16 17 18 19 2 k 1 s-248 27 28 29 21 211 212 B-3 k 2 s-31 s-34 s-27 s-15n s-241 s-26 s-3 Years of measurements 7 6 5 4 3 2 1 Uplift w 27-211 [mm] Fig. 1. Results of the observation of piezometric water level depth in Borehole B-3 and of benchmark uplifts after leak plugging in the Mina drift Fig. 1. Wyniki obserwacji g boko ci zwierciad a wody w otworze B-3 i wypi trzenia reperów po zamkni ciu wycieku w poprzeczni Mina

Ground uplift after closure of water leaks in the Mina drift of the Wieliczka Salt Mine 19 The secondary effect of the reinstatement of the previous hydro-geological conditions may include temporary increase of the rock mass activity. It is visible on the upper salt mine levels. Previously subsiding drifts were uplifted above the Mina drift after 27. Survey of surface ground displacements indicated that the process of reinstatement has not been completed in comparison to the status existing before water penetration. The uplifts resulting from pressure increase in the water lled caverns will stop only after complete disappearance of the depression funnel and clay swell ending. Those processes will be indicated by uplift and subsidence stopping, similarly to the stopping of subsidence before 1992. We should emphasize, however, that the in ux of water to the catchment area drained until 27 was not large, while the leak amounted to ca. 12 17 l/min in the Mina drift. A limited in ux was the basic circumstance which allowed miners to put leaks under control after 1992. Consequently, with the same in ux rate, the period of lling of the drained catchment area will take many years, and long-term ground movements can be expected. SUMMARY AND CONCLUSIONS 1. Water penetration into the Mina drift in 1992 caused serious threat to the salt mine and the lands situated on the mine s northern foreground. After leak plugging in 27, water in ux was stopped, and small regular uplifts were noticed on the surface on the areas of previous subsidence. in reference to previous subsidence, we presented in our paper the distribution of land uplifting and how they are related to hydro-geological and geo- -mechanical conditions. 2. Ground movements have been controlled since leak plugging by annual benchmark height measurements, using the precise levelling method whose mean error does not exceed ±1 mm. 3. The uplifting trough is situated on the area of previous subsidence, with its centre located north of the railway line. Maximum 27 211uplifts reached +63 mm, and the trend indicates that the process will continue in the next years to come. The trough has the shape of an elongated ellipse whose longer side is situated over the sandstone outcrop. 4. The displacements observed on the land surface show the accumulation of : pressure changes taking place in the suffosion caverns that developed during uncontrolled water ow, the displacements effect resulting from the depression funnel lling and watering of previously dried formations, especially clays, in the Chodenice sandstone areas, regular in uence of mine workings convergence which were accounted for in the calculations of the actual ground uplift. 5. Uplift slowing and appearance of subsidence, with the distribution similar to that observed before water penetration into the Mina drift, will indicate the conclusion of the process of reinstatement of previous hydro-geological conditions after leak plugging. The authors would like to thank the managers of the Wieliczka Salt Mine for their kind assistance in giving access to documentary and archival materials.

2 A. Maj, G. Kortas & P. Ulmaniec REFERENCES Bromowicz A. & Brudnik K., 1987. Raport z wykonania programu prac dla likwidacji zagro- enia wodnego od wycieku WIV-27 w poprzeczni Mina. Archiwum Dzia u Geologicznego Kopalni Soli Wieliczka SA (typescript). Garlicki A. & Wilk Z., 1993. Geologiczne i hydrogeologiczne t o awarii na poziomie IV kopalni soli Wieliczka. Przegl d Geologiczny, 3, 1993, 183 192. Garlicki A. & Szybist A., 1995. Ogólne za o enia dla zabezpieczenia Kopalni Soli Wieliczka oraz nowy obraz geologiczny z o a wielickiego. Materia y z III Spotkania Polskiego Stowarzyszenia Górnictwa Solnego Likwidacja zagro enia wodnego dla zabezpieczenia Kopalni Soli Wieliczka. Gonet A., Brudnik K. & Stryczek S., 1997. Zabezpieczenie Kopalni Soli Wieliczka przed zagro eniem wodnym w otoczeniu poprzeczni Mina. Bezpiecze stwo Pracy i Ochrona rodowiska w Górnictwie, Miesi cznik WUG, 12 (4), 2 27. Kortas G. (red.), 24. Ruch górotworu i powierzchni w otoczeniu zabytkowych kopal soli. Wydawnictwo Instytutu Gospodarki Surowcami Mineralnymi i Energi PAN, Kraków. Kortas G. & Maj A., 211. Analiza wraz z interpretacj wyników pomiarów deformacji powierzchni w zwi zku z wyciekiem Mina w Kopalni Soli Wieliczka w aspekcie ochrony powierzchni. Archiwum Dzia u Mierniczego Kopalni Soli Wieliczka SA (typescript). Na cki T., 1995. Warunki hydrogeologiczne. W: Mazurkiewicz M. (red.), Kompleksowa koncepcja zabezpieczenia zabytkowej kopalni soli Wieliczka przed zagro eniem wodnym. Studium mo liwo ci likwidacji zagro enia wodnego dla zabytkowej kopalni soli Wieliczka za pomoc bariery drena owej lub ekranu izoluj cego. Projekt Badawczy Zamawiany nr PBZ 66-1, Archiwum Dzia u Geologicznego Kopalni Soli Wieliczka (typescript). d Obyrn K. & Przyby o J., 21. Rozpoznanie geologiczne z o a soli kamiennej Wieliczka do 1945 roku. Przegl d Górniczy, 3 4, 11 121. Studium mo liwo ci likwidacji zagro enia wodnego dla zabytkowej kopalni soli Wieliczka za pomoc bariery drena owej lub ekranu izoluj cego. Projekt Badawczy Zamawiany nr PBZ 66-1, Archiwum Dzia u Geologicznego Kopalni Soli Wieliczka (typescript). Ulmaniec P., 24. Badanie deformacji powierzchni terenu nad wyciekiem Mina na poziomie IV kopalni wraz z interpretacj wyników. Wieliczka. Streszczenie Wdarcie wód do poprzeczni Mina na IV poziomie Kopalni Soli w Wieliczce w 1992 r. spowodowa o powstanie znacznych deformacji na pó nocnym przedpolu kopalni. Uj cie wycieku i uszczelnienie górotworu pozwoli o na opanowania zagro enia kopalni, a w 27 r. na zamkni cie wycieku. Procesy deformacji górotworu i powierzchni terenu od czasu wyst pienia wdarcia wód do chwili obecnej kszta towane s przez pierwotne i wtórne warunki hydrogeologiczne

Ground uplift after closure of water leaks in the Mina drift of the Wieliczka Salt Mine 21 w utworach warstw chodenickich (Fig. 1). Zamkni cie wycieku w 27 r. rozpocz o proces przywracania naturalnych warunków hydrogeologicznych: podnoszenia poziomu wód z wype nianiem pustek, nawadnianiem zdrenowanych utworów i odbudowaniem naturalnych ci nie. Wp yw tego procesu na ruchy terenu nadal jest obserwowany. Pomiary niwelacyjne na pó nocnym przedpolu z o a prowadzone s od lat 2. ubieg ego wieku. Zag szczon sie dla obserwacji skutków niekontrolowanych przep ywów wód za o ono po pojawieniu si intensywnego wyp ywu w 1992 r. Gwa towne ruchy terenu osi ga y 14 cm/dob (reper S-5 i potem S-3). Po 1993 r. teren obni a si z nierównomiern, ale malej c pr dko ci od 25 mm/rok do 2 mm/rok (Fig. 2, 3), a do zamkni cia wycieku. Od 27 r. teren systematycznie si wypi trza (Fig. 3). Maksymalne wypi trzenia w 29 r. zaobserwowano na reperach S-27 i S-31: +33 mm. Izolinia +1 mm w okresie 27 29 r. obj a prawie ca y obszar zasi gu osiada ponad 1 mm z okresu obserwacji w latach 1992 27 (Fig. 4). Do jesieni 211 roku wypi trzenia wynios y +63 mm, jednocze nie zasi g izolinii +1 mm nieznacznie si powi kszy (Fig. 5), a obj to wypi trze osi gn a warto ok. 2.3 tys. m 3. Wypi trzenia obserwowane s na wszystkich reperach w rejonie niecki sufozyjnej (Fig. 6). W pro lu niecki 1992 27 dominuj skutki gwa townych i znacznych obni e spowodowanych odwadnianiem górotworu i sufozj w latach 1992 1993 (Fig. 7). W pierwszym roku obserwacji wypi trze niecka wykszta ca a si po obu stronach toru kolejowego, nad centrum obni e w poprzednim okresie oraz nad wychodn piaskowców. W kolejnych latach centrum po udniowe zanika, a maksima wypi trze sytuuj si nad piaskowcami z charakterystycznym wyd u eniem formy niecki w kierunku rozci g o ci piaskowców. Obserwowane przemieszczenia pionowe s sum wypi trzania wywo anego odbudow zwierciad a wodnego i obni ania terenu wynikaj cych z zaciskaniem wyrobisk kopalnianych. Po uwzgl dnieniu poprawki na sta e osiadanie terenu wywo ane równomiern konwergencj wyrobisk rzeczywiste warto ci wypi trze spowodowanych wype nianiem si leja depresji wód s wi ksze (Fig. 8). Wprowadzenie tej poprawki prowadzi do zmiany rozk adu wypi trze (Fig. 9) i wzrostu obj to ci podnoszonych mas do V w = 2.6 tys. m 3. Obj to pustek pierwotnych i powsta ych w trakcie wynoszenia materia u skalnego oszacowano na V p =11.5 tys. m 3, zatem stosunek obj to ci niecki wypi trze do obj to ci pustek wynosi V w /V p =.23. Z pomiarów poziomu zwierciad a wody w otworze B-3 wynika, e w trakcie wype niania si leja depresji wyst powa y dwie odr bne pr dko ci podnoszenia poziomu wody. Pocz tkowo, po likwidacji rury D-1, pr dko ta wynosi a k 1 = 8 m/rok. Pó niej, po zamkni ciu zasuwy na rurach D-2 i D-3, pr dko spad a do k 2 = 3 m/rok (Fig. 1). Zmiana tych pr dko- ci odzwierciedla si tak e w wypi trzeniach reperów. Wypi trzenia spowodowane s spr yst reakcj mechaniczn wywo an wzrostem ci- nienia na ciany pustki, rosn cego proporcjonalnie do wysoko ci zwierciad a wody, a tak e efektem wyporno ciowym. Inn przyczyn jest p cznienie utworów, szczególnie i ów, spowodowane ich namakaniem. W pierwszym roku centra obni e i wypi trze pokrywaj si,

22 A. Maj, G. Kortas & P. Ulmaniec wi c dominuj c sk adow wypi trze by y skutki reakcji mechanicznej. Potem centrum niecki wypi trze przesuwa si na pó noc. Powodem tego mo e by wype nianie p ytko rozmieszczonych pustek na wychodniach piaskowców, ale d ugotrwa o procesu wskazuje, e dominuj ce mog by skutki namakania poprzednio zdrenowanych i osuszonych utworów. Symptomem zako czenia procesu przywracania warunków hydrogeologicznych po zamkni ciu wycieku b dzie spowolnienie wypi trze i pojawienie si osiada o rozk adzie podobnym do obserwowanego przed wdarciem wód do poprzeczni Mina.