The Presence of Geogenically Saline Waters in the Area of Salt Dome Rogóźno (Central Poland)

2016, vol. 42 (3) 289–310

The presence of geogenically saline waters in the area of salt dome Rogóźno (central Poland)

Michał Górecki, Maciej Ziułkiewicz

University of Lodz, Faculty of Geographical Sciences, Laboratory of Geology; ul. Narutowicza 88, 90-139 Łódź, Poland; e-mail: [email protected], [email protected]

© 2016 Authors. This is an open access publication, which can be used, distributed and reproduced in any medium according to the Creative Commons CC-BY 4.0 License requiring that the original work has been properly cited.

Received: 13 June 2016; accepted: 22 September 2016

Abstract: Rogóźno salt dome is one of the most recognizable diapirs in the Polish Lowland. Despite its shallow occurrence depth, increased salinity has not been detected in surface water. The presented hydrogeochemical research aimed at determining if there is the presence of increased geogenical salinity in the groundwater and shallow water. Increased geogenical salinity has not been detected in the Moszczenica River and the Czerniaw- ka River, but were displayed in the Moszczenica River valley in the specific electrical conductivity (SEC) spatial distribution. Hydrogeochemical research indicated the presence of a higher mineralized water ascent in the north-eastern part of the dome. The presence of mixing of saline waters around the dome with fresh waters was determined. Ionic composition and hydrochemical indexes of waters sampled from different levels indicate that the saline structure is not completely isolated from surrounding waters. The dome structure is in contact with water from Upper Jurassic formation which influences the final water composition. Active anthropogenic processes partly mask the influences of geogenic salinity in the study area.

Keywords: Rogóźno salt dome, geogenical saline waters, hydrochemical indexes, the Moszczenica River

INTRODUCTION Jodłowski 1997). The presence of saline waters and salt brewing in the area of Łęczyca and Solca Wiel- Late Permian (Zechstein) salt deposits in Central ka the Łódzkie voivodeship have been dated as Poland occur as domes, pillows, walls and dia- early as the 13th century (Fig. 1) (Jodłowski 1977), pirs, with a height of up to 7 km (Czapowski & and continued in Solca Wielka and Pełczyska until Bukowski 2012). Elastic salt masses, due to local the 18th century (Kolago 1965). Natural leakage of disturbances in overburden, started moving to- saline waters in these areas has also been observed wards the surface in the Upper Trias (Tarka 1992). in contemporary times. Intensive settlement and The dome in Rogóźno is one of the diapirs in the highly-developed metallurgical and milling activ- Łódzkie voivodeship which completely broke ity was documented in the Iron Age and Middle through Upper Mesozoic formations (Fig. 1) (Stel- Ages in the Moszczenica River valley, which is the maszczyk 1972, Czapowski & Bukowski 2012). Al- biggest river flowing over the central part of the though it was recognized as one of the biggest salt dome. Pottery, cinders and metallurgical prod- domes of the Polish Lowlands (Tarka 1992), it has ucts, as well as remains of mills and smithies were not yet been effectively recognized in geological found, for example in Gieczno, Rogóźno, Besie- terms (Czapowski & Bukowski 2009). kierz (Fig. 1) (Kamiński 1993). The first informa- Natural leakage of saline waters has been ob- tion about bigger towns located in the dome area served in shallow areas of saline formations (e.g. comes from the period between the 14th and 16th in Inowrocław or Ciechocinek – see Tarka 1992, century (Dylik 1948, Tynenski et al. 2007). There

http://dx.doi.org/10.7494/geol.2016.42.3.289 ISSN 2299-8004 | e-ISSN 2353-0790 | Wydawnictwa AGH 290 Górecki M., Ziułkiewicz M.

is no evidence of the use of saline water in thearea The aim of this research, apart from recog- of dome, both in the archeological material and nizing chemical features of groundwater in the historical documents. Currently, there is no natu- Rogóźno area, was to analyze the spatial varia- ral flow of saline waters in this area as well. bility of surface water chemistry over the saline Soil chemical features also provide evidence of structure. This type of surface water analysis being influenced by salinity from saline diapirs. has not yet been conducted on saline structures. Typically saline soil is not common in the Rogóźno Based on the results, an attempt was made to es- area. In the Łódzkie voivodeship it is present only tablish whether saline water from the dome area in the previously described areas of saline natural could have been mixed with groundwater and flows around Łęczyca, Pełczyska and Solca Wielka surface water. The Moszczenica River valley lo- (Czerwiński 1996, Hulisz 2007a, 2007b). cated over the salt dome, along with surround- Halophytes, which are plants growing in waters ing hydrographic features (ponds, ditches, oxbow of high salinity, confirm higher soil salinity. Nu- lakes) provide very good conditions for conduct- merous areas of halophytes were present in the are- ing such analyses. as of Łęczyca and Ozorków (Fig. 1) until the second half of the 20th century. Currently, the smaller pres- GEOLOGICAL SETTINGS ence of halophytes is preserved around Pełczyska (Kucharski 2009, Mróz 2010). The presence of sa- Rogóźno salt dome is located in the Kuyavian-Po- line areas with halophytes in the salt dome area was meranian anticlinorium. It was formed similiarly recognized only in the 60’s of 20th century around to the Łódź sinclinorium – as a result of folding Rogóźno and Gieczno. Its presence was, most like- during older phases of Alpine orogeny and halo- ly, a short-term occurrence related to drilling pro- tectonics (Turkowska 2001). The Rogóźno diapir jects conducted in the area at that time (Jaworski is the center of the anticlinal structure which is 1964). The flow of drilling fluids and saline waters surrounded by Mesozoic structures (Fig. 1). The could have occurred along poorly insulated drilling dome borders Jurassic structures from the north- holes. The effect of the salt dome on the chemical east, whereas from the south-west it borders Cre- composition of local water has been documented taceous formations. The anticline of Rogóźno over the saline structure of Uścikowo (Prochazka continues in a SE direction, where in the core 1970), and in the area of Rogóźno in the 50’s and there is a sequence of embankments around the 60’s (Jaworski 1964). dome.

Fig. 1. Geological map of Rogóźno and surrounding areas (after Marek 1957; simplified)

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In the plan view, the dome has an ellipsis-like bottom of the formation being more diversified shape, with a longer axis extending in the NW- than formation top (Klatkowa 1993). Quaternary SW direction which is almost along the anticlino- residues cover continuously the entire area with rium of Central Poland (Stelmaszczyk 1972). Rock a layer of variable thickness (Turkowska 2001). salt in Rogóźno is composed of 97.8% of NaCl; The Quaternary residue thickness over the dome estimated rock salt resources to the maximum also varies greatly. Such diversity of thickness is depth of 1000 m have been calculated at 8.6 tril- a reflection of the elevation variability of the Ter- lion tons (Czapowski, on-line). The saline struc- tiary top, and more levelled present topographic ture has a volume of around 120 km3 (Tarka 1992). surface. Additionally, xenolithes, floes of Tertiary The thickness of the cap over the salt dome formations, marlstones and chalky limestones are Rogóźno varies from 13 m in the northern part among the Quaternary formations. They are most to 286 m in the south-eastern part (Stelmaszczyk commonly present in areas of intensive glaciotec- 1972). Gypsum-anhydrite residuum was found in tonic disturbances (Klatkowa 1993). the central part, whereas loam and gypsum were Mesozoic formations protect the salt pillar found on its borders (Jaworski 1962). In the gyp- from dissolution. The contact between the salt sum-anhydrite part, karst processes developed and Mesozoic residue is strictly tectonic. There greatly. Karstification of the cap already occurred, is a fault-flexure dislocation along the south and most probably in the younger Tertiary. It is evi- south-western border of the dome. It cuts and denced by the discontinuous layers of Eocene lig- covers Mesozoic formations (from Trias to Low- nite present in only some of the sinkholes. Also, er Cretaceous-Valanginian). The dislocation zone layers of Miocene lignite are discontinuous and on the east border of the dome is slightly lower. they are only present in a few more significant Residues of Upper Jurassic are in discordant con- depressions. It is evidence that the karstification tact with Zechstein formations, starting from of the cap was not completed in the Tertiary, but Kimmeridgian (Stelmaszczyk 1972). The Juras- also continued in Pleistocene and may also have sic is represented by the Late Jurassic limestones. continued to occur in modern times. The process There are Quarternary outcrops of Upper Juras- of the karstification of the cap contributed to the sic limestones (Klatkowa 1993) in the Gieczno and surface modification of the glacial till of the War- Besiekierz area (the eastern and northern side of ta. The deep buried forms and present valley of the the dome). Late Jurassic limestones on the western Moszczenica River are related to karst processes side of the diapir are covered with the overhang of taking place in the gypsum-anhydrite cap, espe- loam-gypsum cap and a thin layer of Lower Creta- cially in its central part (Kamiński 1993). There is ceous which was only detected on the western and a co-dependancy observed between the course of southern border of the dome (Stelmaszczyk 1972). river valley and lowering in ceiling of Tertiary residuum. It is possible that deep and narrow erosive HYDROGEOLOGICAL indentations in clay are related to karst lowering AND HYDROLOGICAL SETTINGS in the dome cap, repeated in the following geological periods (Kamiński 1993). Aragonite, a min- Intense tectonic, saline, glaciotectonic disturbanc- eral rarely present in Poland and which has never es or karstification occuring in the area of the salt been found in any saline residue of Polish Low- dome contribute to a complicated circulation sys- lands, was found in Rogóźno. Aragonite is, most tem of groundwater flow. In some areas, ground- probably, evidence of gypsum leaching (Jaworski water flow of highly-mineralized water from deep- 1962); after all, the process of leaching is especially er aquifers is displayed in the near-surface water intense in the environment reach in saline waters flow system. There is a local, direct contact -be (Pazdro & Kozerski 1990). tween aquifer Quaternary formation with Tertiary Cenozoic residue, which is present over the sands in Gieczno area (Miocene and possibly old- loam-gypsum alluvium, includes formations from er) (Stelmaszczyk 1972). Water from Quaternary the Paleogene, Neogene and Quaternary. The and Tertiary aquifers in the Rogóźno area are so thickness of formations, previously classified as interconnected that they might be considered to be Tertiary, greatly varies in the cap basin; with the one Miocene-Quaternary aquifer.

Geology, Geophysics and Environment, 2016, 42 (3): 289–310 292 Górecki M., Ziułkiewicz M.

Fig. 2. Documentation map of Rogóźno region

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Fig. 3. Area of possible ascent of groundwater from Tertiary formation against the system of hydroisobaths of the first deep Quaternary level

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Contact between this aquifer and water from Per- River and Czerniawka River are characterized with mian formation (Dokumentacja..., 2002) is proba- moderetaly developed nival regime which, in this ble. The Miocene level, connected with sands sep- area, is characterized by balanced groundwa- arating layers of lignite from different eras had, ter and surface flow components in total outflow most probably, a hydraulic contact with a salt de- (Jokiel 2004). The highest flow in these rivers is posit (Stelmaszczyk 1972) connects with ground- noted at the turn of March and April, and the low- water from the Permian formation. Groundwa- est at the turn of September and October (Mak- ter around the dome (Permian system) may be symiuk 2001). accumulated in voids and fractures between the A little over 1/3 of the Moszczenica River length saline water table and a dense gypsum cap. The and over 1/2 of the Czerniawka River lenght are lo- gypsum cap is, most likely, not always in direct cated in the area of salt dome Rogóźno. Apart from contact with the saline water table and it creates Moszczenica and Czerniawka rivers, there are a ceiling above washed-out parts of the salt dome. nameless surface streams in the area, with the total Frequently the higher part of residuum occurs as length of about 3 km. In the dome area, the densi- chaotic debris of gypsum and anhydrite with res- ty of river system is relatively higher and amounts idues of salt, gypsum marlstone and loam. Such to about 0.579 km∙km−2 (Szaniawski 1963), which rubble, containing many empty voids, can be par- means it is similar to the maximum amount in tially or completely filled with eluvial silt up be- Central Poland –0.6 km∙km−2 (Jokiel 2004). fore it becomes a compact rock mass. Saline water can be accumulated when these voids are com- METHODOLOGY OF FIELD pletely filled with sediment (Szaniawski 1963). RESEARCH ON SURFACE WATERS There is lateral contact between water from Upper Jurassic aquifer and saline water from Zechstein The analysis of hydrochemical conditions around aquifer behind the northern and north-western the Rogóźno salt dome was conducted in selected border of the dome (Meszczyński & Szczerbicka observation points on the following rivers: the Mo- 2002). The high temperature of water from the szczenica River, the Czerniawka River and their Upper Jurassic aquifer indicates flow system from tributaries. Selection of sample-control points was a greater depth that eventually accumulates in Ju- performed strictly according to Inspectorate of rassic limestones. Because of the neighboring salt Environmental Protection regulations (Gołębio- dome, limestones were piled, disturbed tectoni- wska et al. 1994), taking into consideration spec- cally and cracked. Covered with an impermeable ificity of local conditions. 14 water samples were loam-gypsum cap, they became a suitable reser- collected: seven from the Moszczenica River, two voir for accumulating warm water flowing from from the Czerniawka River and one of each of the below (Stelmaszczyk 1972). tributaries (Fig. 2, Tab. 1). Water temperature (T), The analysis of the Quaternary and Tertiary hy- pH and SEC were measured at every point. Ad- droisobaths is indicated in areas of Władysławów ditionally, water levels (H) were monitored in the and Lorenki potential ascent zone (Figs. 2, 3) gauge station of the Institute of Meteorology and (Górecki 2015). Water Management in Moszczenica-Gieczno. The Moszczenica River serves as a draining Other hydrographic features in Moszczenica base level of shallow aquifer flow systems. Aqui- River valley include oxbow lakes and mires, and fers, present in Quaternary formations, form a lo- artificial ponds and ditches. Spatial distribution cal water circulation system while deeper aquifers of SEC was used to evaluate total mineralization (Tertiary and Upper Jurassic) form a regional sys- changes in all types of surface waters as this pa- tem draining to the Bzura River valley on WNW rameter is a good indicator of changes in the water from the dome (Bierkowska & Błaszczyk 1989). chemical composition (Witczak et al. 2013). Hy- Moszczenica is the biggest river draining the drochemical mapping was conducted at the end northern part of the Łódź Hills. It is 56 km long of August 2014 a period characterized by low-flow and is a tributary of the Bzura River. Czerniaw- regime (Fig. 4). Measurements were taken in riv- ka, its biggest tributary, flows into the Moszczeni- ers and streams with continuous flow as well as ca River in the Rogóźno area (Fig. 2). Moszczenica in non farming ditches and ponds (Fig. 2, Tab. 2).

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Table 1 Characteristics of measurement points along the rivers

Geographical Number Name of the river, coordinates Lenght [km] Description of a location of point watercourseA (N, E)A 51°55'55.3'' I Moszczenica 30+500 a bridge in Michałów 19°28'40.2'' 51°58'08.1'' II Moszczenica 23+400 before mouth the Czerniawka River in Kotowice 19°26'35.4'' 51°58'13.1'' III Moszczenica 23+300 after mouth the Czerniawka River in Kotowice 19°26'34.1'' 51°58'42.4'' IV Moszczenica 22+200 a meander in Kotowice 19°26'29.7'' 51°59'49.0'' V Moszczenica 19+500B a stream gauge in Gieczno 19°26'35.2'' 52°00'34.2'' VI Moszczenica 17+700 a bridge in Borowiec 19°26'27.4'' 52°01'15.5'' VII Moszczenica 15+900 a bridge on the dirt road in Sypin 19°26'42.4'' 51°55'54.2'' VIII nameless watercourse 0+400 a culvert under the road in Wola Branicka 19°28'25.8'' 51°57'11.2'' IX Czerniawka 1+800 a bridge on the voivodeship road 708 in Bądków 19°26'33.2'' 51°58'07.1'' before mouth into the Moszczenica X Czerniawka 0+100 19°26'33.3'' River in Kotowice 51°57'15.5'' XI nameless watercourse 0+400 a culvert under the voivodeship road 708 in Bądków 19°26'21.1'' 51°57'35.5'' XII creek with Jasionka 0+200 a bridge on the dirt road in Kotowice 19°26'20.8'' 51°58'31.9'' XIII oxbow Moszczenica 0+400 a bridge on the road in Kotowice 19°26'44.4'' 52°00'32.8'' XIV Dezerta 4+100 a bridge on the dirt road in Borowiec 19°26'07.1'' Explanations: number of point according to Figure 2; A – based on Czarnecka 2005; B – lenght for the stream gauge in Gieczno (based on Szczepański 1995–1996).

Fig. 4. Water level (H) in the Moszczenica River in Gieczno during period October 2014 –November 2015

Geology, Geophysics and Environment, 2016, 42 (3): 289–310 296 Górecki M., Ziułkiewicz M. Description of a locationof ditch pond/peatbog pond pond the Moszczenica River ditch the Moszczenica River the Czerniawka River ditch the Moszczenica River pond (N, E) 51°58'17.2'' 51°57'11.2'' 51°59'27.7'' 51°58'31.9'' 51°58'32.1'' 51°57'15.5'' 51°58'13.5'' 19°26'21.1'' 51°57'59.7'' 19°28'29.1'' 51°56'32.2'' 51°59'26.7'' 51°58'30.8'' 19°26'44.4'' 19°25'46.8'' 19°26'55.6'' 19°26'55.5'' 19°26'33.2'' 19°25'30.9'' 19°26'28.5'' 19°27'02.3'' 19°27'22.0'' coordinates Geographical Geographical 31 33 32 27 35 29 25 28 30 26 34 of point Number Description of a locationof ditch the Moszczenica River the Moszczenica River ditch pond ditch pond the Dezerta River pond pond the Moszczenica River pond (N, E) 51°59'51.1'' 51°59'49.0'' 51°59'07.0'' 52°01'15.5'' 19°26'07.1'' 51°58'43.5'' 19°27'47.7'' 19°28'40.1'' 19°28'41.9'' 19°26'27.4'' 51°58'42.7'' 19°25'43.9'' 19°26'15.0'' 19°26'42.4'' 52°00'30.1'' 52°00'55.5'' 19°26'35.2'' 19°25'38.8'' 19°25'54.0'' 19°27'58.7'' 52°00'32.8'' 52°00'20.2'' 52°00'34.2'' 52°00'04.5'' coordinates Geographical Geographical 14 16 17 18 21 19 15 13 22 23 24 20 of point Number Description of a locationof the Moszczenica River pond ditch pond ditch pond the Moszczenica River pond ditch pond pond pond (N, E) 19°28'17.1'' 19°29'17.4'' 51°55'55.3'' 51°56'59.5'' 51°57'39.4'' 19°29'37.4'' 51°57'09.9'' 19°29'41.8'' 19°29'19.9'' 51°56'03.8'' 51°55'54.2'' 51°58'32.6'' 51°58'05.7'' 51°57'30.8'' 51°58'04.9'' 51°56'06.8'' 51°58'28.3'' 19°29'03.4'' 19°28'40.2'' 19°29'23.5'' 19°28'32,4'' 19°28'25.8'' 19°28'54.5'' 19°28,00.4'' coordinates Geographical Geographical

5 6 1 7 3 4 2 8 9 11 10 12 of point Number Table 2 Table Mapping sites of specific electrical conductivity(SEC) Explanations: number of point according to Figure 2.

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METHODOLOGY concentration of chloride ions (Fig. 5). Sever- OF FIELD RESEARCH al- or dozen times higher concentration of Cl− in ON GROUNDWATER comparison with the higher limit may indicate the presence of migration of saline water into the The initial analysis of hydrogeochemical condi- near-surface area. tions in the dome area was conducted on the ba- In order to establish the scale of salinity of sis of data coming from 65 hydrogeological obser- groundwater and its origin, the hydrogeologi- vation points (piezometers and wells). The main cal documentation and marked zones of upward source of information was the HYDRO Bank data flow of mineralized waters into surface (Fig. 3) base of the Polish Hydrogeological Survey and the was used. A group of hydrogeological formations archives of Department of Geology and Geologi- was selected for the research. The respective crite- cal Concession of the Marshal Office of Łódzkie ria were taken into consideration while choosing Voivodeship. Collected hydrochemical data came suitable wells: from the following formation: Quaternary (45 cas- −− whether accumulated waters indicate higher es), Tertiary (11), Upper Jurassic (6) and Permian value of total mineralization or chlorides, residue (3). A relationship between the Cl− con- −− the close or nearby location of hypothetical centration and water total mineralization in water zones of saline waters (Fig. 3), from Tertiary and Upper Jurassic formations with −− technical condition enabling the possibility of the R2 value close to unity was observed. sampling. Based on archive data, the chloride baseline of According to the criteria above, six wells and water from Quaternary formation for Rogóźno two piezometers were selected (Fig. 2, Tab. 3). salt dome was established (n = 45). The boundary One pond was also included as, according to for the baseline was the concentration of Cl− cor- archival data, it was close to the possible up- responding to the difference between one standard ward flow area of the saline waters, strictly con- deviation and estimated parameter median value nected to a nearby drilling hole. Well and pond (68% of observation) (Zdechlik & Kania 2003). sampling included measurements of water tem- The lower limit of chloride baseline is 7 mg∙dm−3, perature (T), pH, SEC and reduction-oxidation whereas the higher 90 mg∙dm−3. potential (Eh). An overflow chamber was used in Some of the wells accumulating water from the measurement to protect the water from con- the Quaternary formation display an anomalous tact with air.

Cl– [mg ∙ dm–3] (mbgl) avg D

Fig. 5. Change in concentration of chloride ion (Cl−) in groundwater from Quaternary formation (D) in the area of Rogóźno salt dome with respect to the upper margin of the local hydrochemical chloride baseline

Geology, Geophysics and Environment, 2016, 42 (3): 289–310 298 Górecki M., Ziułkiewicz M. User “Gieczyńska” former water intake poultry farm “Janisz” petrol station “Markie- Pol” firm former milk- collection former agricultural cooperative “Salio” horse- riding club private personprivate “Moya” petrol“Moya” station – – – – – – + + + Artesian flow Allocation not innot use irrigation observation of groundwater quality innot use innot use not innot use n.d. pond observation of groundwater quality J J J J – Q Q Q Q Age aquifer of – [m] n.d. 1.5–5.0 Filtering 16.2–18.0 35.0–39.0 52.0–70.0 69.5–103.0 56.6–150.0 238.5–241.4 compartment – 6.2 n.d. 41.0 18.5 70.0 103.0 241.4 150.0 Depth well of [m] 51°59'45.1'' 51°59'27.6'' 51°57'27.8'' 51°58'13.5'' 51°58'13.5'' 52°00'17.9'' 51°57'14.3'' well (N, E) 51°58'42.6'' 51°59'35.3'' 19°30'49.3'' 19°27'07.4'' 19°28'57.7'' 19°27'14.6'' 19°25'33.0'' 19°26'55.5'' 19°28'12.5'' 19°29'28.5'' 19°26'54.6'' Geographical Geographical coordinates of – – – 5 910 356 5 910 5 900 618 5 900 371 5 900 412 5 900 325 5 900 348 to CBDH Number of well according I F E B C A G D H

Number to Figureto 2 of wellof according Explanations: – Central CBDH Hydrogeological Databank (Centralna Baza Danych Hydrogeologicznych); n.d. data; – no Q – Quaternary; J – Upper Jurassic Table 3 Table Characteristics of groundwater and surface water sampling points

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Na+ METHODOLOGY −− [6] Sodium Adsorption Ratio: SARSAR = ()Ca22+++ Mg /2 OF LABORATORY RESEARCH expresses relative activity of sodium in exchange reactions with the water impact on soil. Apart from the measurement of physicochemical The higher the index, the easier it is for Na+ to parameters in situ, samples of water for laboratory transfer to a sorption complex. At the same analysis were taken in order to evaluate the pres- time, the probability of high soil salinity in- ence of the following ions: creases. The parameter the alkalinity of water −− in the case of water sampled from river: Cl− and + as well (Kwaterkiewicz & Sadurski 1986, Och- Na ; man et al. 2011, Singh et al. 2014). −− in the case of groundwater and the pond: an- − − − − 2− 3− It was assumed that if the areas of higher wa- ions (Cl , HCO3 , NO3 , NO2 , SO4 , PO4 ), + + + 2+ 2+ 2+ 2+ ter total mineralization and higher concentra- cations (Na , K , NH4 , Ca , Mg , Mn , Fe ), tion of chloride ions overlap with areas where and a total amount of dissolved substances of the upward flow of water from deeper levels, the total carbonate and non-carbonate hardness. salt dome influences water chemistry in the Mo- Six hydrochemical ratio indexes were used to szczenica valley. The interpretation of the ion interpret the chemical composition of groundwa- composition of groundwater on the basis of hy- ter: [1] sodium vs. chloride, [2] sodium vs. sodium drochemical indexes allowed the origin of salinity and chloride, [3] calcium vs. magnesium, [4] bi- to be determined. carbonate vs. chloride, [5] ESP (Exchange Sodium Percentage), and [6] SAR (Sodium Adsorption Ratio) (e.g. Macioszczyk 1987, Hounslow 1995, RESULTS Razowska 1999). Their calculation was based on the content of ions in the equivalent form. Local hydrological conditions during field stud- Na+ −− [1] Sodium vs. chloride index: Cl− establishes ies refer to Moszczenica River level on the wa- the level of water metamorphosis and its iso- ter gauge in Gieczno in the range of 130–147 cm lation from the area, as well as from other aq- (Fig. 4) which, according to Szczepański 1995, is uifers. With the lowering of the index, water a low level. These numbers correspond to the river becomes older and the levels of metamorpho- flow from 0.62 m3∙s−1 to 1.06 m3∙s−1 (according to sis and isolation become higher (Macioszczyk the Institute of Meteorology and Water Manage- 1987, Pazdro & Kozerski 1990). ment); which represent average level in this part of −− [2] Sodium vs. sodium and chloride index: the river (Szczepański 1995). Na+ Na+−+ Cl along with water total mineralization The minimum and maximum values of exam- helps determining the sources of sodium in ined physico-chemical parameters observed on water (Hounslow 1995). measure-control gauges are represented in Table 4. Ca2+ −− [3] Calcium vs. magnesium index: Mg2+ helps There is a continuous pattern in examined phys- in establishing if low-mineralized groundwater ico-chemical parameters of water in the middle are contaminated by calcium or magnesium course of the Moszczenica River. Prior to connec- fertilizers (Macioszczyk 1987). tion with the tributary Czerniawka River, the aver- − HCO3 −− [4] Bicarbonate vs. chloride index: Cl− as- age statistical water chemistry data and their range sess length of the flow of water from the re- were relatively high. After the waters are combined, charge area. A low value of the index means the parameters are lower and the range between water staying in the rock formation for a longer them is reduced, then increased again in the lower time (Winid & Lewkiewicz-Małysa 2005). part of the Moszczenica River (Fig. 6A–C). −− [5] Exchange Sodium Percentage: The analyzed SEC area in surface waters under- ()Na+++⋅K 100 ESP = 22++++% ESP Ca ++Mg Na + K establishes the useful- goes important changes (Fig. 7). The area of low- ness of water for irrigation purposes. Water er than 400 µS∙cm−1 is located along Moszczenica with high ESP index may contain colloids and River channel and the upper part of Czerniawka suspensions which have a negative effect on River. SEC of surface waters increases with a grow- soil permeability (Singh et al. 2014). ing distance from the Moszczenica River.

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60 A

40 ] –3 30 [mg ∙ dm –

Cl 20

0 I II X III IV V VI VII

24 22 B 20 18 16 ] –3 14 12 [mg ∙ dm

+ 10

Na 8 6 4 2 0 I II X III IV V VI VII

600 C

550

] 500 –1

450

SEC [µS ∙ cm 400

350

300 I II X III IV V VI VII

Fig. 6. Statistical distribution of chloride ion (Cl−) in measure-control points in the Moszczenica and the Czerniawka rivers (A); statistical distribution of sodium ion (Na+) in measure-control points in the Moszczenica and the Czerniawka rivers (B); statistical distribution of specific electrical conductivity (SEC) in measure-control points in the Moszczenica and the Czerniawka rivers (C)

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Fig. 7. Changes in conductivity (SEC) of surface water in the Rogóźno region

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Table 4 Minimum and maximum values of selected hydrochemical elements of examined rivers in selected measure-control points

pH SEC [µS∙cm−1] Cl− [mg∙dm−3] Na+ [mg∙dm−3] Objects (n) min max min max min max min max All objects (14) 4.77 8.75 317 639 14.0 49.4 4.9 27.4 Points on the Moszczenica River (7) 7.11 8.75 375 579 25.4 49.4 12.3 22.0 Points on the tributaries of the 4.77 8.54 317 639 14.0 45.5 4.9 27.4 Moszczenica River (7)

The highest value of the parameter SEC is observed in the direction of the Warsaw-Ber- (913 µS∙cm−1) was observed in the pond locat- lin glacial valley, on the western side of the Mo- ed in Rogóźno. High conductivity contributes to szczenica River. the identification of an anomaly area around the Hydrogeochemical characteristics of sampled pond, within larger area of relatively consistent objects are presented in Kurlov formula (Tab. 5); spatial variability of SEC. Gradual increase of SEC supplemented with information on water pH.

Table 5 Chemical analysis of sampled objects on the basis of Kurlov formula

Number of well Kurlov formula

A �� HCO� Cl SO� NO� �� M �� T , pH Ca Na Mg K B �� Cl HCO� SO� � �� M �� T , pH Na Ca Mg K C �� NO� SO� Cl HCO� �� M �� T , pH Ca Mg Na K D �� HCO� Cl SO� NO� �� M �� T , pH Ca Na Mg K NH� E �� HCO� Cl SO� �� M �� T , pH Ca Na Mg K F �� HCO� Cl SO� �� M �� T , pH Ca Na Mg K G �� HCO� SO� Cl NO� �� M �� T , pH Ca Mg Na K H �� Cl HCO� SO� �� M �� T , pH Na Ca Mg K I �� Cl HCO� SO� � �� M �� T , pH Explanations: number of well accordingCa Na to Figure Mg 2 Kand Table 3.

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Groundwater, with semi-acid pH, flows into high. Correlation between concentrations of Na+ the shallowest piezometers. The ionic composition and Cl− is good, particularly at high concentra- of these waters indicates their relative similarity. tions. In the central and northern stretch of the The important difference is shown with respect to Moszczenica River, which is within the salt dome a dominant anion. Bicarbonates are dominant in area and outside its northern border, there was no water sampled from piezometer (A) whereas ni- significant increase of measured physicochemical trates are dominant in water flowing into the pi- parameters (Fig. 6A–C) while significantly higher ezometer (C). salinity was observed in its tributary, the Dezerta Quaternary deep wells (D, E) are recharged River. The Moszczenica River, in contrast to other with waters that do not have total mineraliza- rivers in the region, is characterized with average tion higher than 600 mg∙dm−3; they consist main- SEC and concentration of Cl− ion, which suggests ly of bicarbonates, chlorides, calcium and sodium. relatively the limited influence of the anthropo- Other ions are present, but in small concentra- genic impact on the water chemistry (Ocena stanu tions and the temperature and pH of these waters wód powierzchniowych, 2013). are similar. SEC overall increases with a increasing dis- Wells collecting water from Upper Jurassic tance from the Moszczenica River and the Czer- formations can be divided into two groups. Each niawka River respectively (Fig. 7). This spatial of these groups is characterized by unique physi- regularity is disturbed by certain ‘anomalous’ co-chemical parameters. The first group consists zones. Elevated SEC anomalies around towns of of wells (G) and (F). Water flowing into them is Władysławów and Lorenki overlap with areas of alkaline and of low total mineralization. Water possible ascent of water from Tertiary formation in the well (F) is bicarbonate-calcium dominated (Fig. 3) (Górecki 2015). The results obtained from by significant concentrations of Cl− and Na+. This the hydrochemical analyses may suggest the pres- well has an artesian flow of about 1.7 dm3∙s−1 and ence of certain zones where saline groundwater temperature of 24.0°C. The second group con- coming from the area around the dome are flow- sists of wells (B) and (H). In each of the wells, the ing up to the surface. groundwater table is stabilized above the surface. Six ionic ratios have been calculated based on In (B) the artesian uplift reaches 0.18 m, whereas measured parameters and used to interpret pro- in (H) it is about 4.8 m with the simultaneous out- cesses influencing water chemistry in specific ob- flow of water with temperature of 24.0°C. Mineral servation points (Tab. 6). The location of the pie- chloride-sodium waters flow into the well; where- zometers (A), (C) next to gas stations, residential in higher rate of calcium is present in the well (H). areas or farmlands influences groundwater chem- The chemical analysis indicates that in the pond istry. Water sampled from the well (A) showed (I) there is a slightly acidic acratopegae and its Cl− concentration of over 42 mg∙dm−3 (Tab. 5). In − − + 2+ main components are: Cl , HCO3 , Na and Ca . comparison with the archive data coming from piezometers, the concentration is higher but it is DISCUSSION within the range of the hydrochemical baseline which does not point to any anomalous rates of Increased flow volumes of the Moszczenica River ions in water. The ratio between potassium and correlated with decreased pH (R2 = 0.7; Fig. 8A) sodium is low values and may be an evidence of and an increased concentration of Na+ (R2 = 0.6; an anomaly in the aquifer. Other evidence of the Fig. 8B). There is no observable statistically signif- anthropogenic impact are the elevated concen- 2− 3− − icant correlation between flow volume and SEC trations of SO4 , PO4 and NO3 . The low pH of and Cl− concentration, which could be caused water is connected to the presence of sulfates in by diverse sources of Cl− (Mazurek 2000). Dur- the quantity bigger than 20% mval. Permanent ing high flows, some of the smallest and biggest anthropogenic contamination of water is prov- rates of SEC and Cl− were observed. The correla- en by the presence of all mineral forms of nitro- − + − − tion between conductivity and Cl ion in water is gen (NH4 , NO2 , NO3 ), increased content of ni- observed only when concentration of Cl− is very trogen, phosphates and sulfates (Macioszczyk &

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Dobrzyński 2002) and cause low values of ionic confirmed in the low value of the HCO3/Cl ratio, ratio Na/Cl (index 1), which falsely suggest the which is shown in a low content of bicarbonates presence of a very good and long-lasting isola- (Tab. 5). The low pH of water may be linked to the − tion from the surface which classifies groundwa- anomalous content of NO3 (Pazdro & Kozerski ter as relict, highly metamorphosed. High values 1990) while the lack of an impermeable layer and of ionic ratio HCO3/Cl (index 4) in contrast, rep- the shallow presence of groundwater contributes resent waters in the active recharge zone. Con- to the high level of oxidation-reduction poten- tamination of groundwater might be indicated tial (Eh = 238 mV). However, the environment is by ionic ratio HCO3/Cl. Water sampled from the transitional, between oxidising and reducing with −3 − well (C) contains 176 mg∙dm of NO3 ion, which relatively low pH in the aquifer (Tab. 5) (Witczak strongly suggests water contamination. This is also et al. 2013).

A pH

Q (m3 ∙ s· –1)

B ) –3 dm

· ∙

(mg + Na

Q (m3 ∙ s·–1)

Fig. 8. Correlation between the water flow (Q) and its pH reaction (pH) on Gieczno water gauge (A); correlation between the water flow (Q) and sodium ion content (Na+) on Gieczno water gauge (B)

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Table 6 Characteristics of groundwater and surface waters on the basis of hydrochemical indicators

Number of object Indicator Interpretation A B C D E F G H I very good insulation X X X X X Na+ good insulation X X X − Cl no insulation X halite solution X1 Na+ sodium source other than halite X 1 Na+−+ Cl brine X X X X X anthropopressure X X X

Ca2+ contamination X X X 2+ Mg no contamination X X X X X X minimal recharge X X − HCO3 transistion zone X X Cl− active recharge X X X X X suitable for irrigation X X X X X X X ESP unsuitable for irrigation X X risk of soil salinity X X X SAR no risk of soil salinity X X X X X X

Explanations: number of object according to Figure 2, Table 3 and Table 5; 1 – ratio value allows for classification into two classes.

The high value of ionic ratio Na/Cl and low waters of high salinity around the salt dome. The value of ionic ratio HCO3/Cl indicate waters iso- ion balance (Tab. 5) and values of hydrochemical lated from the surface; such waters have a diffi- indexes (Tab. 6) suggest that water in the well has cult contact with surface and infiltration waters. characteristic features of both waters typical for However, groundwater is present approximately the active recharge zone and of waters influenced 2 m b.g.l with no isolating aquifer (the archive of by anthropological and geogenic factors. Inter- the Łódzkie Voivodeship Marshall Office, cata- pretation of ionic ratios is difficult because of in- logue number 1094). The low result of Na/Na+Cl terference between anthropogenic contamination ratio (index 2) with increased total mineralization and geogenic contamination. The chemical com- also improperly characterizes this water as saline position and ionic ratio ssuggest that water in the originating from geogenical salinity. This waters well (E) is a combintation of highly mineralized shows signs of contamination. waters mixed with natural groundwater from the The deeper and shallow aquifers are hydrau- active recharge zone. High concentration of Cl− lically connected, something which was observed (136 mg∙dm−3), accompanied by high concentra- during pumping test in well (D), when flow oc- tions of Na+ (Tab. 5) suggests a geogenically saline curred from one aquifer to another. The shallow water. In contrast to well (D), ion balance of the aquifer is not isolated from the surface and is vul- well water does not indicate that the Quaternary nerable to contamination. Bicarbonate and calci- aquifer is in hydraulic contact with the first shal- um ions overall are dominant ions but Cl− and Na+ low aquifer, as it was in well (D). The environment ions are also present in high concentrations. Con- in the aquifer is slightly reducing (Witczak et al. centration of Cl− of 70 mg∙dm−3 in groundwater 2013). Values of the ionic ratio Na/Na+Cl (in- from Quaternary formation in the Rogóźno area is dex 2) suggest a possible influence of the salt dome high, but not above the baseline range. Increased on the water chemistry (Tab. 6). The ionic ratio concentration of Cl− and Na+ indicates that wa- Na/Cl (index 1) informs about good isolation of ters flowing into the well may be in contact with the aquifer from the surface with only limited

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contact with infiltration water. However, along (Pazdro & Kozerski 1990). The conditions in the with the presence of Na+, a risk of soil salinity is water are transitional, between oxidizing and represent (index 5). The ion composition of water ducing with unusually high pH (10.7). It is a rare sampled from wells (D) and (E), as well as hydro- occurrence that such an alkaline would be caused chemical indexes confirm the possibility of up- by geogenical factors (Witczak et al. 2013). There ward water flow (geogenically mineralized wa- is no indication of any present contaminations, ter) from deeper aquifers indicated in Figure 3 and possibly such a high pH is caused by natural- (Górecki 2015). ly occuring conditions. The hydrochemical type Well (B) is located right outside the north- of water and ionic ratios (Tab. 6) may confirm, ern border of the salt dome. The chemical anal- as in case of the well (B), mixing of saline and ysis indicated that there are two ions dominat- natural groundwater. However, the ionic coming in the water: Cl− and Na+ (Tab. 5). The high position suggests that natural groundwater has concentration of these ions is characteristic for a significantly higher impact in this mixture. It is deep groundwater influenced by the leaching indicated in confirmed with relatively low con- of rock salt or other evaporites (Macioszczyk & centration of Cl− and Na+, low water total min- Dobrzyński 2002, Witczak et al. 2013). Indirect eralization and ionic ratios Na/Cl and Na/Na+Cl, contact of water with saline rocks is also indicat- respectively. The ionic ratio HCO3/Cl is typical ed by its high total mineralization. The water is for waters of active recharge zone; it is also indi- slightly alkaline (Tab. 5) and has low value of ox- cated by carbonate hardness (Pazdro & Kozerski idizing-reducing potential (Eh = −518 mV). Re- 1990). Value of ratios ESP (index 5) and SAR (in- ducing the environment causes the minor partic- dex 6) enables the water to be used for irrigation 2− ipation of reduced concentrations of SO4 which with no risk of increased salinity in the aquifer. undergoes reductions and enriches water in H2S Well (G) is located outside the eastern border of (Macioszczyk & Dobrzyński 2002). Despite re- the salt dome. The low concentration of chlorides ducing conditions, the concentration of sulfates and sodium suggests that there is no contact with in water amounts to 110 mg∙dm−3 which, in com- waters flowing over the salt dome (Tab. 5). Ratios parison with other water from the Upper Juras- Na/Cl and HCO3/Cl inform us about the presence sic aquifer that were analyzed, is high. The disso- of waters in the active recharge zone (Tab. 6). It is lution of evaporites rich in this ion may provide also indicated by the carbonate hardness (Pazdro a significant amount of sulfates. However, there is & Kozerski 1990). Lack of contamination flow no increased concentration of K+ or Mg2+ (Pazdro is indicated by the ratio Ca/Mg. There are three & Kozerski 1990) which are, frequently, related to dominant ions in the sample (H): Cl−, Na+ and the process. The slates confining the deeper aqui- Ca2+ (Tab. 5). The concentration of the chloride fer could contribute to higher concentrations of anion amounts to over 408 mg∙dm−3, and sodium 2− −3 SO4 . The possibility of the salt dome influenc- cation to over 206 mg∙dm . The increased value ing water chemistry is expressed in low values of of Ca2+ in the saline water may be caused by ion ionic ratio HCO3/Cl (index 4), characteristic for exchange. It occurs when high NaCl waters are in saline waters (Tab. 6). The ionic ratio Na/Na+Cl contact with carbonate rocks. This type of water is (index 2) (about 0.5) informs us that the sodi- frequently present in deep hydrogeological struc- um in water comes from dissolution of halite. tures (Pazdro & Kozerski 1990). Water in the out- The well is currently used occassionally, only in flow has a temperature of 24.0°C so, just like in the the event of long drought periods to irrigate the case of water from the well (F), which is classified surrounding area. A high concentration of Na+ in as hypothermal waters. The total dissolved solids comparison with other cations means the water amounts to more than 1 g∙dm−3, which classifies would be unusable for irrigation (index 5). Any this water as having a relatively low mineral con- one using such water for irrigation may result in centration (Pazdro & Kozerski 1990) in the poor- increased soil salinity (index 6). Upper Jurassic ly reductive environment (Witczak et al. 2013). aquifers derived through the well (F) are located This water flows from a neglected well through under a thick sequence of impermeable rocks. The a narrow stream, into a nearby meadow and fi- water temperature in the outflow reaches 24.0°C nally into a ditch. The surrounding area is en- (Tab. 5), which is classified as hypothermal waters dangered with the contamination of the soil and

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the shallow aquifer due to improper protection Cl− (Tab. 5). High concentrations of Cl− and Na+ of self-flowing saline waters. The ratio Na/Na+Cl suggest the inflow of geogenically saline waters. characterizes water as saline water which, accord- A minimum presence of mineral forms of nitrogen ing to the ratio Na/Cl, is very well isolated from and phosphorus confirms natural, instead of an- the surface area (Tab. 6). The ratio HCO3/Cl con- thropological salinity (Górski 2001, Macioszczyk firms the good isolation from surface water. The & Dobrzyński 2002, Witczak et al. 2013). Increased high total mineralization and content of chlorides concentration of K+ and Mg2+ may suggest the in- and sodium causes the water to be unusable for flow of contamination from fertilizers. However, irrigation (index 5). In the Rogóźno area, ground- due to lack of any other signs of anthropopression, water from the Upper Jurassic formation contact it is very likely that the source of these ions can be with a saline structure – a hydraulic barrier that found in leaching of potassium-magnesium salts. also causes modifications in physico-chemical Surface water in the pond may mix with saline composition of the flowing water. The influence water, which flows through a nearby unsealed ex- of salt dome on water from Upper Jurassic aqui- ploration hole. A similar situation in groundwa- fer is found in the ion composition of groundwater is observed in wells (D), (E) and (F), respec- ter derived from wells located on opposite sides. tively. According to archive documentation of the Groundwater derived from wells (F) and (G) do Marshal Office of Łódzkie Voivodeship, there had not indicate any contact with the salt dome. On been a few piezometers near the pond in the past, the other side of the diapir, there is a high geogen- characterized by very high concentration of chlo- ical influence of saline rocks on physico-chemical ride and sodium ions. The presence of not properly composition of groundwater in wells (B) and (H). maintained well H-4 located close to the pond may There are four ions dominating the sur- cause the inflow of saline waters into the surface. face water in the pond (I): Ca2+, Na+, HCO− and A similar situation occurs in the outflow (H).

Fig. 9. Piper diagram with results of chemical analyses of groundwater and surface waters

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The location of points on the Piper diagram inflow of both natural and saline waters to them. (Fig. 9) confirms areas of presence of genetical- The water in the pond (I) is also influenced by ly different waters: natural, saline, transitional geogenical salinity – however, on a slightly great- (natural and saline waters mixing with each other scale than it is in the context of Quaternary er), as well as waters affected by anthropopres- wells. A similar example of salinization of sur- sion. In the case of water from the Upper Jurassic face waters was presented by Drwal & Borowiak aquifer, the difference between natural water (F), (2000). (G) and saline water (B), (H) is very clear – the Using Ogilvy method (Kiełczawa 2000), a chart points are groupped in two zones located on the showing the process of water mixing in selected opposing sides of every chart (E side, N-W side). wells and piezometers is shown in Figure 10. The Wells from deep Quaternary formation (D), (E) rate of determination factor (R2) close to unity sig- are grouped between saline and natural wa- nifies very high correlation between the minerali- ter from Upper Jurassic aquifer which indicates zation of water and the content of ions.

Fig. 10. Ogilvy chart showing the mixing of water in the area of Rogóźno salt dome

CONCLUSIONS 2. The salt dome is located along the groundwater flow direction of Upper Jurassic formation The research and analysis of surface water and in the regional drainage zone. It is supported groundwater show the following: by the completely different ion composition of 1. Rogóźno saline structure is not complete- water on opposite sides of the diapir. ly isolated from surrounding waters. Tecton- 3. The pond (I) and wells (D) and (E) are located ic, saline, glaciotectonic and karst process- within the area of increased SEC values which es influence the entire complicated system of surrounds the salt dome. A mixing of min- groundwater circulation. eralized geogenical waters and waters from

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shallow aquifers is present within Quaternary Drwal J. & Borowiak M., 2000. Chemizm wód powierzchnio- formation. These areas are influenced by saline wych w strefie kontaktu lądu i morza. [in:] Burchard J. (eds.), Stan i antropogeniczne zmiany jakości wód w Pol- water from around the salt dome. sce, Wydawnictwo Uniwersytetu Łódzkiego, Łódź, 91–100. 4. The increased SEC in surface waters is present Dylik J., 1948. Rozwój osadnictwa w okolicach Łodzi. Acta behind the northern border of the dome. The Geographica Universitatis Lodziensis, 2, Łódzkie Towa- rzystwo Naukowe, Łódź. influence of the salt dome on surface water is Gołębiowska K., Niespodziewany A. & Reczek T., 1994. expressed in high values of SEC and concen- Wskazówki metodyczne do projektowania regionalnego tration of Cl− and Na+ in the Dezerta River. monitoringu wód powierzchniowych płynących. Biblioteka Monitoringu Środowiska, Państwowa Inspekcja Ochrony 5. The Moszczenica River is influenced by saline Środowiska, Warszawa. waters either through tributaries (the Dezerta Górecki M., 2015. Chlorki jako wskaźnik geogenicznego zasole- River) or saline waters in ditches in the area of nia wód powierzchniowych i gruntowych na obszarze wysadu solnego Rogóźno [M.Sc. thesis]. Repozytorium Uniwer- Władysławów and Lorenki. sytetu Łódzkiego, Łódź, [on-line:] http://dspace.uni.lodz. 6. Anthropogenic influence is reflected in anoma- pl:8080/xmlui/handle/11089/16858 [access: 13.06.2016]. lies of physico-chemical parameters of ground- Górski J., 2001. Propozycja oceny antropogenicznego zanie- water observed in piezometers. czyszczenia wód podziemnych na podstawie wybranych wskaźników hydrochemicznych. [in:] Bocheńska T. & Staśko S. (red.), Współczesne problemy hydrogeologii. T. The authors would like to thank the Reviewers: 10, cz. 1, “Sudety”, Wrocław, 309–313. Marek Matyjasik, Ph.D. and Dorota Porowska, Hounslow A.W., 1995. Waret Quality Data. Analysis and In- terpretation. Lewis Publishers, New York. Ph.D. for their suggestions which helped us to im- Hulisz P., 2007a. Wybrane aspekty badań gleb zasolonych prove the manuscript. w Polsce. Stowarzyszenie Oświatowców Polskich, Toruń. Hulisz P., 2007b. Propozycje systematyki gleb zasolonych występujących w Polsce. Roczniki Gleboznawcze, 58, 1/2, REFERENCES 121–129. Jaworski A., 1962. Aragonit w utworach czapy wysadu solnego w Rogóźnie koło Łodzi. Przegląd Geologiczny, 10, 11, Bierkowska M. & Błaszczyk J., 1989. Objaśnienia do Mapy hy- 592–595. drogeologicznej Polski w skali 1:200 000. Państwowy In- Jaworski A., 1964. Powierzchniowe przejawy zasolenia na ob- stytut Geologiczny, Warszawa. szarze wysadu solnego w Rogóźnie koło Łodzi. Przegląd CBDH (Centralna Baza Danych Hydrogeologicznych, System Geologiczny, 12, 3, 148–149. Przetwarzania Danych Państwowej Służby Hydrogeolo- Jodłowski A., 1977. Badania archeologiczne nad początkami gicznej), 2014. Państwowy Instytut Geologiczny – Pań- eksploatacji soli w Polsce środkowej. Sprawozdania Ar- stwowy Instytut Badawczy, Warszawa. [on-line:] http:// cheologiczne, 29, 179–187. spdpsh.pgi.gov.pl/PSHv7/ [access: 14 February 2014]. Jokiel P., 2004. Zasoby wodne Środkowej Polski na progu Czapowski G., Surowce chemiczne. Sole kamienne i sole po- XXI wieku. Wydawnictwo Uniwersytetu Łódzkiego, Łódź. tasowo-magnezowe. Rogóźno. Państwowy Instytut Geolo- Kamiński J., 1993. Późnoplejstoceńska i holoceńska transfor- giczny – Państwowy Instytut Badawczy, Zakład Geologii macja doliny Moszczenicy jako rezultat zmian środowiska Gospodarczej. [on-line:] http://surowce-chemiczne.pgi. naturalnego oraz działalności człowieka. Acta Geographi- gov.pl/sole_Rogozno.htm [access: 13.06.2016]. ca Lodziensia, 64, Łódzkie Towarzystwo Naukowe, Łódź. Czapowski G. & Bukowski K., 2009. Złoża soli w Polsce – stan Kiełczawa B., 2000. Zmienność mineralizacji wód gór- aktualny i perspektywy zagospodarowania. Przegląd Geo- nokredowych Gorzanowa. Przegląd Geologiczny, 48, 12, logiczny, 57, 9, 798–811. 1195–1199. Czapowski G. & Bukowski K., 2012. Salt resources in Poland Klatkowa H., 1993. Objaśnienia do Szczegółowej mapy geolog- at the beginning of the 21st century. Geology, Geophysics icznej w skali 1:50 000. Arkusz Zgierz. Państwowy Instytut & Environment, 38, 2, 189–208. Geologiczny, Warszawa. Czarnecka H. (red.), 2005. Atlas podziału hydrograficznego Kolago C., 1965. Perspektywy balneologiczne Łodzi. Przegląd Polski. Cz. 1, Mapy w skali 1:200 000. Atlasy Instytutu Geologiczny, 13, 8, 350. Meteorologii i Gospodarki Wodnej, Instytut Meteorolo- Kucharski L., 2009. Naturalna i półnaturalna roślinność gii i Gospodarki Wodnej, Warszawa. nieleśna. [in:] Kurowski J.K. (red.), Szata roślinna Polski Czerwiński Z., 1996. Zasolenie wód i gleb na terenie Kujaw. środkowej, Wydawnictwo EKO-GRAF, Łódź, 81–102. Roczniki Gleboznawcze, 47, 3/4, 131–143. Kwaterkiewicz A. & Sadurski A., 1986. Problem genezy wód Dokumentacja hydrogeologiczna określająca warunki hy- zmineralizowanych w sąsiedztwie Jeziora Żarnowieckiego. drogeologiczne w związku z projektowaniem stacji dys- Annales Societatis Geologorum Poloniae, 56, 1–2, 163–177. trybucji paliw płynnych na dz. nr 127/1 w Rogóźnie. Macioszczyk A., 1987. System oceny jakości i stopnia zanie- Archiwum Urzędu Marszałkowskiego Województwa czyszczenia wód podziemnych eksploatowanych do ce- Łódzkiego (dok. 1068), 2002 [unpublished]. lów pitnych. Przegląd Geologiczny, 35, 12, 628–636.

Geology, Geophysics and Environment, 2016, 42 (3): 289–310 310 Górecki M., Ziułkiewicz M.

Macioszczyk A. & Dobrzyński D., 2002. Hydrogeochemia stre- Groundwater of Ranchi Township Area, Jharkhand, In- fy aktywnej wymiany wód podziemnych. Wydawnictwo dia. Current World Environment, 9, 3, 804–813. Naukowe PWN, Warszawa. Stelmaszczyk Z., 1972. Ogólna charakterystyka hydrogeolo- Maksymiuk Z., 2001. Wody. [in:] Liszewski S. (red.), Zarys giczna obszaru Rogóźna. Archiwum Wydziału Geolo- monografii województwa łódzkiego, Łódzkie Towarzy- gii i Koncesji Geologicznych Urzędu Marszałkowskiego stwo Naukowe, Łódź, 60–68. Województwa Łódzkiego, Łódź [M.Sc. thesis]. Marek S., 1957. Wstępne rozpoznanie stratygraficzne dolnej Szaniawski H., 1963. Wyjaśnienie stosunków wodnych w rejo- kredy w obszarze Rogóźna i Ozorkowa. Geological Quar- nie wysadu solnego Rogóźno. [in:] Dębski J., Podemski M. terly, 1, 2, 247–258. & Szaniawski H. (red.), Dokumentacja geologiczna złoża soli Mazurek M., 2000. Zmienność transportu materiału rozpusz- kamiennej w wysadzie solnym Rogóźno, pow. Łęczyca, woj. czonego w zlewni Kłudy jako przejaw współczesnych pro- Łódź, Państwowy Instytut Geologiczny, Warszawa, 38–51. cesów denudacji chemicznej (Pomorze Zachodnie). Wy- Szczepański W. (red.), 1995. Atlas posterunków wodowskazo- dawnictwo Naukowe UAM, Poznań. wych dla potrzeb państwowego monitoringu środowiska: Meszczyński J. & Szczerbicka M., 2002. Objaśnienia do Mapy posterunki wodowskazowe IMGW. Biblioteka Monitorin- hydrogeologicznej Polski w skali 1:50 000. Arkusz Zgierz. gu Środowiska, Państwowa Inspekcja Ochrony Środowi- Państwowy Instytut Geologiczny, Warszawa. ska, Warszawa – Katowice. Mróz W. (red.), 2010. Monitoring siedlisk przyrodniczych: Tarka R., 1992. Tektonika wybranych złóż soli w Polsce na przewodnik metodyczny. Część 1. Biblioteka Monitoringu podstawie badań mezostrukturalnych. Prace Państwowe- Środowiska, Główny Inspektorat Ochrony Środowiska, go Instytutu Geologicznego, 137, PIG, Warszawa. Warszawa. Turkowska K., 2001. Budowa geologiczna i rzeźba terenu. Ocena stanu wód powierzchniowych, 2013. Wojewódzki In- [in:] Liszewski S. (red.), Zarys monografii województwa spektorat Ochrony Środowiska w Łodzi. łódzkiego, Łódzkie Towarzystwo Naukowe, Łódź, 51–60. Ochman D., Kawałko D., Kaszubkiewicz J. & Jezierski P., 2011. Tynenski Z., Właziński Z., Adamska T. & Lesiewicz A., 2007. Zawartość rozpuszczalnych kationów i anionów w wycią- Analiza możliwości wykorzystania zasobów wód geoter- gach wodnych z gleb zasalanych wodami poflotacyjnymi malnych i powierzchniowych oraz borowin w okolicy miej- infiltrującymi ze składowiska „Żelazny Most”. Ochrona scowości Rogóźno dla potrzeb rozwoju turystyki, rekreacji Środowiska i Zasobów Naturalnych, 48, 266–275. i lecznictwa. Centrum Zrównoważonego Rozwoju, Łódź. Pazdro Z. & Kozerski B., 1990. Hydrogeologia ogólna. Wy- Winid B. & Lewkiewicz-Małysa A., 2005. Mineralne wody dawnictwa Geologiczne, Warszawa. lecznicze Iwonicza Zdroju w świetle badań wskaźników Prochazka K., 1970. Wpływ wysadowych struktur solnych Kło- hydrochemicznych. Gospodarka Surowcami Mineralny- dawy i Uścikowa na zasolenie skał nadkładu i wód stu- mi, 21, 2, 49–67. dziennych. Prace Geologiczne – Polska Akademia Nauk. Witczak S., Kania J. & Kmiecik E. (red.), 2013. Katalog wybra- Oddział w Krakowie. Komisja Nauk Geologicznych, 62, nych fizycznych i chemicznych wskaźników zanieczyszczeń Wydawnictwo Geologiczne, Warszawa. wód podziemnych i metod ich oznaczania. Biblioteka Mo- Razowska L., 1999. Wskaźniki hydrochemiczne – mało przy- nitoringu Środowiska, Inspekcja Ochrony Środowiska, datne czy niedoceniane. [in:] Krajewski S. & Sadurski A. Warszawa. (red.), Współczesne problemy hydrogeologii. T. 9, Hydro- Zdechlik R. & Kania J., 2003. Tło hydrogeochemiczne i roz- geologia na przełomie wieków, Warszawa–Kielce 15–17 kład stężeń jonów wskaźnikowych w rejonie złoża Beł- września 1999, Państwowy Instytut Geologiczny, War- chatów. [in:] Kozerski B. & Jaworska-Szulc B. (red.), szawa, 307–313. Współczesne problemy hydrogeologii. T. 11, cz. 2, Wydział Singh P., Kumar Tiwari A. & Kumar Singh P., 2014. Hy- Budownictwa Wodnego i Inżynierii Środowiska Poli- drochemical Characteristic and Quality Assessment of techniki Gdańskiej, Gdańsk, 327–334.

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