Recession Subregimes of Karstic Springs Discharge and their Manifestation in Oxygen Isotopes Content

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1 Recession Subregimes of Karstic Springs Discharge and their Manifestation in Oxygen Isotopes Content Peter Malík 1, Juraj Michalko 2 & Jaromír Švasta 3 1 State Geological Institute of Dionýz Štúr, Mlynská dolina 1 Bratislava, Slovakia, peter.malik@geology.sk 2 State Geological Institute of Dionýz Štúr, Mlynská dolina 1, Bratislava, Slovakia, juraj.michalko@geology.sk 3 State Geological Institute of Dionýz Štúr, Mlynská dolina 1, Bratislava, Slovakia, jaromir.svasta@geology.sk Abstract Forested hills of the Brezovské Karpaty Mts. (max. 585 m a.s.l. of altitude), neighbouring the northern Slovakian part of the Vienna Basin, are built mainly by karstified Middle and Upper Triassic dolomites and limestones. In the period of , groundwater quality of four karstic springs was monitored in 20-days intervals including sampling for δ 18 O (SMOW) oxygen isotopes. Temporal stability of chemical components contents in groundwater was evaluated as very stable during the whole observation period, as only small deviations were observed in chemical macrocomponents contents. On the contrary, spring discharges showed typical karstic behaviour (steep peaks during the snow-melting period, very low discharges during summer and autumn droughts). Also analyses of springs recession curves had revealed presence of several subregimes, including turbulent ones. Within this study, various stages of the spring's recession curve - flatter parts for groundwater draining small fissures, steeper parts for groundwater circulating in more opened fissures or karst conduits were described by superposition of series of equations. Subsequently, proportional amounts of different discharging subregimes were calculated. Groundwater, discharging at individual springs, was considered as a mixture of various groundwater types; maybe originated as different subregimes, each of which can be characterised characterised e.g. by δ 18 O (SMOW) values. Proportional representation of individual subregimes discharge on the total discharge leads to both δ 18 O and groundwater temperature forecast for pure subregime in the case of e.g. the Vítek spring, the water outflowing in 2 nd laminar subregime seems to be both more depleted in δ 18 O ( %), and colder in temperature values (9.66 C), in comparison to the 1 st laminar baseflow ( % / C). Data calculated for turbulent subregimes seem to be unrealistically exaggerated in calculated water temperatures, but maybe suggest on contact with the uppermost part of the aquifer affected by sun radiation. Obtained results are based only on sparsely populated datasets and manual discharge records, but seem to represent a perspective method for future interpretations. In the future, also groundwater chemical properties can be processed in the same way. Keywords: groundwater, oxygen isotopes, hydrograph analyses, recession curves, Brezovské Karpaty Mts., Slovakia Introduction A significant prospective resource of uncontaminated high-quality potable water in Western Slovakia is represented by limestone-dolomite complexes of the Brezovské Karpaty Mts. (Fig. 1). Forested hills of the Brezovské Karpaty Mts. (max. 585 m a.s.l. of altitude), neighbouring the northern Slovakian part of the Vienna Basin, are built mainly by karstified Middle and Upper Triassic dolomites and limestones. Mesozoic carbonate rocks of the Brezovské Karpaty cover 77.4 km 2, but with the adjacent (possibly drained) area the groundwater basin can be extended to km 2, and involves not only the mountain range itself but also its wide surroundings. The average altitude of the whole area is m above sea level and that of the Triassic carbonate range m a.s.l. (Malík et al. 1992). Therefore, these structures of outcropping limestones a dolomites belong, together with the Čachtické Karpaty Mts. (294.9 m) among the lowest-lying karst-fissure hydrogeological structures in the West Carpathians. In the centre of the area, ancient municipality named Dobrá Voda (Good Quality Water in translation) designates the regional importance from the drinking groundwater supply point of view (Fig. 2). Triassic limestones and dolomites of the Jablonica Group (Salaj et al. 1987) form the principal environment of groundwater formation and circulation. All limestone and dolomite formations of this group are highly permeable and, from a regional point of view, make up a single unit, although its permeability is variable. Carbonate permeability is generally very high, but there are considerable differences between limestones and dolomites (Guttenstein/Annaberg, Schreyeralm, Steinalm, reifling,

2 Ramin, Wetterstein, Opponitz and Dachstein limestones versus Wetterstein Dolomites and Hauptdolomites; Began et al., 1984). The limestones are characterized by fissure-karst and fissure premeability. In contrast, fissure and/or fissure-porous permeability of relatively more rigid dolomites resulted from their tectonic fracturing. The ratio of the outcropping dolomites prevails: they form more than two thirds (68.9 %) of Mesozoic carbonates, while uncovered area of limestones (24.1 km 2, e.i %) is substantially smaller. This fact is reflected in a relatively low number of caves registered in Brezovské Karpaty Mts. (Bella et al. 2007). Amidst a m thick massif of Middle and Upper Triassic dolomites and limestones there is a fairly thin (5 10 m) horizon of sandstones and shales - the Lunz beds - which is the only impermeable formation in the Jablonica Group. It acts as a barrier as well as impermeable substratum separating individual groundwater circuits and significantly influencing their direction. One should note, that no swallow holes ponors appear in the whole area of the Brezovské Karpaty Mts., and groundwater is recharged purely by effective (unevaporated) precipitation. Fig.1: Position of the investigated area Brezovské Karpaty Mts. (Slovakia) Although superficial karstic features are seldom to be found in the Brezovské Karpaty Mts., several major groundwater outlets with typical karstic behaviour (outflow concentration into several tens or even hundreds of litres per second, steep peaks during the snow-melting period, very low discharges during summer and autumn droughts) are present, implying underground karstification. Springs related to dolomites are characterized by one or two laminar subregimes of discharge (with low α 1 and α 2 values sensu Malík, 2007); = 1 to day -1 ; α 2 = 1 to day -1. Groundwater outflows from a karstified limestone environment have usually two laminar discharge subregimes characteristic for a more heterogeneous aquifer (α 1 ranges from day -1 to day -1, α 2 from day -1 to day - 1 ), but with limited manifestations of turbulent effects on groundwater flow (Malík et al. 1992). From the viewpoint of groundwater quality protection, the limestone environment is more vulnerable as possible contamination can spread more quickly, and self cleaning capacity for contamination is very limited. In contrast, groundwater in dolomites, due to their detailed extensive fracturing and pore-fissure permeability, may be contaminated less intensively, but for longer periods. The average specific runoff 9.98 l s -1 km -2 (315 mm) from the outcropping Triassic carbonates in the Brezovské Karpaty Mts. does not correspond to climatic and hydrogeological settings of the area it is maybe by some l s -1 km -2 higher than was inferred from analogy with surrounding mountains. The runoff from the territory of the carbonate structures exceeds the amount of percolated precipitation by some 359 l s -1 in total. The excessive runoff can be explained by hidden inflow from the surrounding Upper Cretaceous and Neogene sedimentary strata formations (sandstones, siltstones, conglomerates) to carbonate structures (Malík et al. 1992). The drainage of the Cretaceous and Neogene clastic sedimentary

3 rocks by underlying carbonates is reflected on the water balance of the whole Brezovské Karpaty Mts. area ( km 2 ). For the whole area, the specific runoff in hydrological year 1988 was 5.74 l s -1 km -2 (181 mm), which is more adequate to its position on the continent (E17 35 ; N48 30 ), the average altitude of m a.s.l and an average precipitation of mm/year. Groundwater from the Mesozoic carbonates can be marked by clearly Ca-Mg-HCO 3 chemical type. T.D.S. content of these relatively uncontaminated sources attains approximately mg l -1, with Ca 2+ ~92.7 mg l -1, Mg 2+ ~32.7 mg l -1 -, NO 3 ~5.0 mg l -1, Cl - ~3.7 mg l -1 -, SO 4 ~29.9 mg l and HCO 3 ~405.2 mg l -1 (average values by Vrana in Malík et al., 1992). Monitoring of groundwater quality and springs discharges In the period of , starting from Nov. 19, 1987, groundwater quality of four karstic springs was periodically monitored in approximately 20-days step (22 samples from each spring, last sample taken on Feb. 28, 1989). All these springs (Chtelnica Vítek; Jablonica Stušková; Prašník Spod javora; Hradište pod Vrátnom Tri mlynky) were bound to karstic aquifers of the Brezovské Karpaty Mts. Another spring Dolný in the Žriedlová dolina near Brezová pod Bradlom, was also observed during the same period of hydrogeological investigations, but as bound to Miocene sandstones, is not discussed within this paper. Spring Tri mlynky in Hradište pod Vrátnom is bound to dominantly dolomitic aquifer, spring Stušková in Jablonica to dominantly limestone aquifer and within the recharge areas of springs Vítek in Chtelnica and Spod javora in Prašník, both limestones and dolomites are present. Discharges of all these spring were simultaneously monitored by the Slovak Hydrometeorological Institute; three from the karstic springs (apart from Jablonica Stušková) were exploited as drinking water sources of regional importance. Basic characteristic of these springs is shown in the Tab. 1, position of the monitored springs on the simplified geological sketch of the Brezovské Karpaty Mts. is on Fig. 2. Tab.1: Basic characteristic of investigated springs in the Brezovské Karpaty Mts. site spring monitored monitored Q min Q avg Q max T min T max since up to [l s -1 ] [l s -1 ] [l s -1 ] Chtelnica Vítek Jablonica Stužková ,0 Prašník Spod javora (Šteruská) ,0 Hradište pod Vrátnom Tri mlynky Žriedlová dolina Dolný The results of these water-quality regime observations suggest a relatively high uniformity of water chemistry throughout the whole period, which is documented mainly by very low variation coefficient of T.D.S. (2.4 to 3.7 %), HCO 3 2- ( %) or Ca 2+ ( %) in waters from these springs. More variable concentrations were noted only in the case of components probably subjected to anthropogeneous impacts variation coefficients of NO 3 - ( %), Cl - ( %), K + ( %) after Vrana in Malík et al. (1992). Studied springs were also sampled and analysed for δ 18 O (in vs. SMOW) oxygen isotope content in all series, data were obtained by measurements in the laboratory of Isotope Geology Dpt., State geological Institute of Dionýz Štúr in Bratislava. Tab.2: Basic results of oxygen isotope analyses water from springs in the Brezovské Karpaty Mts. spring name: Vítek Stužková Šteruská Tri mlynky δ 18 O T date: water δ 18 O T water δ 18 O T water δ 18 O T water [ SMOW] [ SMOW] [ SMOW] [ SMOW]

4 spring name: date: Fig.2: Vítek δ18o Twater [ SMOW] Stužková δ18o Twater [ SMOW] Šteruská δ18o Twater [ SMOW] Tri mlynky δ18o Twater [ SMOW] Simplified geological sketch of the Brezovské Karpaty Mts., position of the monitored springs

5 Fig.3: Time plot of δ 18 O values 4 karstic springs in the Brezovské Karpaty Mts. Results of the monitoring of isotope composition of water, shown on Fig. 3, gave relatively similar (and expectable) results for all the springs. All the values vary from to , with the overall average value of The differences between individual springs seemed to be dependent on relative altitudinal position of springs recharge areas, not too enhanced in the flat hills of the Brezovské Karpaty Mts. The position of springs is very similar an varies from 250 to 275 m of altitude (see Tab. 3). However, altitude of recharge area is slightly more different and a negative correlation effect with the altitude can be found, with the gradient of of δ 18 O values with each 100 m of altitude (correlation coefficient -0.70). Malík et al. (1993) meant some 100 m altitude change with 0.1 of δ 18 O difference for karst springs in the Veľká Fatra Mts. (Slovakia). Tab.3: Basic statistic data on δ 18 O values springs in the Brezovské Karpaty Mts. Spod javora spring name: Vítek Stužková Tri mlynky (Šteruská) spring s altitude 275 m 250 m 250 m 260 m altitude of recharge area 448 m 313 m 348 m 393 m δ 18 O T parameter: water δ 18 O T water δ 18 O T water δ 18 O T water [SMOW] [SMOW] [SMOW] [SMOW] minimum maximum average median standard deviation variation coefficient 2% 8% 1% 6% 2% 93% 1% 21%

6 In the detailed time plot (Fig. 3), the differences in δ 18 O values are evident, as changing with time/discharge of individual springs. The relative distance difference of δ 18 O values between individual springs seem to be steady, while they all vary in time with less or more similar behaviour. However, the differences in their discharges are not the same. As a first interpretation step, δ 18 O values were plotted against discharges (Fig. 3), with slightly contradictory results for different springs. This was previously explained as consequence of differences between groundwater circulation in dolomites vs. limestones (Malík et al. 1992), compare Tri mlynky / dolomitic and Vítek / limestone recharge area on Fig. 4). In the dolomitic aquifer, the oxygen isotopes in water were heavier with increasing discharge (Hradište pod Vrátnom Tri mlynky spring), while in the more karstified limestone in the recharge area of spring Vítek near Chtelnica, the increased volume of discharged groundwater was more depleted in δ 18 O. The observed facts were not so outright (see Fig. 4), but at the time of the investigation ( ) there were not too many possibilities of more detailed interpretations. δ 18 O [ SMOW] Tri mlynky Q [l s -1 ] δ 18 O [ SMOW] Vítek Q [l s -1 ] Fig.4: Values of δ 18 O (SMOW) plotted against discharges of monitored springs Tri mlynky and Vítek Recession curves analyses Although the principles of hydrograph analyses are developed for more than a century (Boussinesq 1877; Maillet 1905), only computerised algorithms enabled its proper and use for distinguishing of different elements in groundwater mixtures (Goldscheider & Drew, 2007). In this study, we are using simple exponential description (Q t = Q o e -α t ) of laminar subregimes as defined by aforementioned authors, and a linear turbulent model for flow supposed to be in karstic channels (Q t = Q o (1-β t)) as described by Kullman (1983). Several both laminar and turbulent subregimes may exist in one aquifer, and its discharge can be described by superposition of several appropriate equations (Kullman 1990). Hydrograph recession curves can be used for analyses of type and properties of a karstic aquifer (Kullman 2000), as well as for estimation of regional karstification degree and groundwater sensitivity to pollution (Malík 2007). In the case of the Brezovské Karpaty Mts., the previous analyses of springs recession curves had revealed presence of several discharge subregimes, including turbulent ones. Various stages of the spring's recession curve - flatter parts for groundwater draining small fissures, steeper parts for groundwater circulating in more opened fissures or karst conduits could be described by superposition of series of equations. In Tab. 4, results of recession curves analyses undertaken on individual springs of the Brezovské Karpaty Mts. are shown, both as individual parameters and resulting equations. Tab.4: Recession curves parameters of investigated springs in the Brezovské Karpaty Mts. α 1 α 2 site spring [day -1 ] [day -1 ] [day -1 ] [day -1 ] recession curve equation (Q in [l s -1 ]) Chtelnica Vítek Q t = e t e t ( t) β 1 Jablonica Stužková Q t = e t e t ( t) Prašník Spod javora (Šteruská) Qt = e t ( t) Hradište pod Vrátnom Tri mlynky Q t = 14.0 e t β 2

7 Fig.4: Plots of typical recession curves of investigated springs in the Brezovské Karpaty Mts., evaluated on the base of assemblage individual recession curves from dry periods Fig.5: Logarithmical plots of typical recession curves of investigated springs in the Brezovské Karpaty Mts., evaluated on the base of assemblage individual recession curves from dry periods

8 Subregimes in hydrograph separation The reverse method of hydrograph separation, after all the subregimes of an aquifer or spring were explicitly defined by equations, can be implemented for determination of e.g. groundwater amounts discharged in individual subregimes. The main principle for developing hydrograph separation tool, based on solution of sequence of equations, is a presumption that the discharge of an aquifer depends on the level of its groundwater saturation, and that the same discharge reflects the same groundwater saturation level. As the exponential equation has no analytical solution, the set of pre-described equations for each real discharge value has to be solved by iteration process to obtain partial discharges for each subregime. The total discharge has to be then the sum of these partial discharges. Subsequently, proportional amounts of different discharging subregimes can be calculated, both for the whole period and for every moment of evaluated period (Tab. 5). Hydrograph separation example for spring Vítek into three individual subregimes (1 st laminar, 2 nd laminar, turbulent) is on Fig. 6 b), total volume of groundwater discharged in individual subregimes, as well as in the whole observation period for all four karstic springs in the Brezovvské Karpaty Mts. is in Tab. 5. a) b) c) d) Fig.6: Vítek spring (near Chtelnica) a) discharge and samplings in hydrological years 1987, 1988 and 1989; b) hydrograph separation into 3 different subregimes; c) samplings and discharges in different subregimes in hydrological years ; d) detailed samplings and discharges in different subregimes in the period Tab.5: Volume of groundwater discharged in individual subregimes in the period of Nov. 01, 1987 Feb. 28, total volume in volume in volume in spring average discharged 1 st laminar 2 nd laminar turbulent discharge volume subregime subregime subregime [l s -1 ] Vítek

9 total volume in volume in volume in average discharged 1 st laminar 2 nd laminar turbulent spring discharge volume subregime subregime subregime [l s -1 ] Stužková Spod javora (Šteruská) Tri mlynky Qualitative differences between hydrograph subregimes The change of groundwater properties of individual springs in time (Fig. 3, Tab. 2) can be linked to mixing of groundwater of different origin. One of the explanations of the temporal δ 18 O (SMOW) values change (and other qualitative groundwater properties, of course) is different proportional representation of individual subregimes in the final mixture. If we assume the slowest groundwater circulation to be present in smallest fissures (1 st laminar subregime), the groundwater present in more widened fissures to be exfiltrated in the 2 nd laminar subregime, and the groundwater circulating in open karstic conduits to be represented by turbulent flow subregimes, we can make an attempt to interpret and reconstruct the groundwater composition of 100 % subregimes. In the Tab. 6, proportional representation of individual subregimes discharge on the total discharge (in %), together with absolute values (in l s -1 ) are listed for the spring Vítek (site Chtelnica). Similar calculation, using equations parameters from the Tab. 4, was performed to obtain subregime discharges for each spring. Based on possible impact proportional representation a subregimes (in %) on the final mixture δ 18 O value ( SMOW), a forecast for 100 % representation of a subregime can be calculated by simple statistics. The same processing was performed with groundwater temperature values (data shown both in Tabs. 2 for all springs, and Tab. 6 for spring Vítek). Results for both δ 18 O and groundwater temperature values in 100 % representation forecast for the 1 st laminar, 2 nd laminar and turbulent subregimes are listed in the Tab. 7. Tab.6: Spring Vítek total discharge and discharges calculated for individual subregimes, with their proportional representation on the total discharge, in the sampling days (Tab. 2; shown on Fig. 6) for δ 18 O. Q date TOTAL Q laminar-1 Q laminar-2 Q turbulent Q laminar-1 Q laminar-2 Q turbulent δ 18 O T water [l s -1 ] [l s -1 ] [l s -1 ] [l s -1 ] [%] [%] [%] [SMOW] % 6.2% 0.0% % 5.3% 0.0% % 6.8% 0.0% % 7.2% 0.0% % 18.1% 18.9% % 19.5% 4.7% % 15.7% 0.0% % 15.3% 0.0% % 12.6% 0.0% % 11.1% 0.0% % 8.8% 0.0% % 7.7% 0.0% % 6.6% 0.0% % 5.7% 0.0% % 4.8% 0.0%

10 Tab.7: 1 st laminar, 2 nd laminar and turbulent subregimes in individual springs discharge: results of the 100 % representation forecast for δ 18 O and groundwater temperature values recharge 1 st laminar 2 nd laminar turbulent without subregimes spring area altitude [m] δ 18 O [SMOW] T water δ 18 O [SMOW] T water δ 18 O [SMOW] T water δ 18 O [SMOW] T water Vítek Stužková Spod javora Tri mlynky minimum maximum average median standard deviation variation coefficient 1% 53% 1% 39% In comparison with Tab. 3, and also with its last two columns, the results for δ 18 O values in 100 % representation forecast in the Tab. 7 for the 1 st laminar subregime are very similar to evaluation without subregimes. The reason is the overall nature of the springs (dolomitic aquifers), as well as character of the recession curves with dominating 1 st laminar subregime. However, results for 2 nd laminar and turbulent subregimes seem to be contradictory in both cases. Groundwater contained in the macrofracture system (2 nd laminar subregime) of the Vítek spring is both more depleted in δ 18 O, and colder in temperature values, in comparison to the 1 st laminar baseflow. The 2 nd laminar subregime in Stužková spring keeps approximately the same value of δ 18 O, but also points to colder circulating groundwater. The only two turbulent subregimes (springs Vítek and Spod javora) seem to be unrealistically exaggerated in water temperatures (calculated data). While in the case of spring Vítek, turbulent flow component was present only in two samplings, in the case of Spod javora spring the turbulent flow component was constantly present see the different character of this spring s depletion on Figs. 4 and 5. It seems that the warmer water present in the possible karst conduits depletion can be more likely in contact with heliothermozone the uppermost part of the aquifer heated by sun radiation. In the case of Spod javora spring, the relatively heavy δ 18 O values can also point to possible evaporation processes in the karst channels. Spring Vítek does not show such behaviour, anyhow the δ 18 O values there are very similar to those in the 2 nd laminar subregime. Obtained results are based only on sparsely populated datasets and manual discharge records, but seem to represent a perspective method for future interpretations. Conclusions Forested hills of the Brezovské Karpaty Mts. (max. 585 m a.s.l. of altitude), neighbouring the northern Slovakian part of the Vienna Basin, are built mainly by karstified Middle and Upper Triassic dolomites and limestones. In the period of , groundwater quality of four karstic springs was monitored in 20-days intervals, including sampling for δ 18 O (SMOW) oxygen isotopes. Temporal stability of chemical components contents in groundwater was evaluated as very stable during the whole observation period, as only small deviations were observed in chemical macrocomponents contents in Ca 2+, Mg 2+ -, HCO 3 macrocomponents contents. More variable concentrations during monitoring were noted only in components probably subjected to anthropogeneous impact (Na +, K +, NO - 3, Cl - and SO 2-4 ; Vrana in Malík et al., 1992). On the contrary, spring discharges showed typical karstic behaviour with steep peaks after the snow-melting periods and very low discharges during summer and autumn droughts. Also analyses of springs recession curves had revealed presence of several subregimes, including turbulent ones. However, by the end of eighties, no PC techniques, nor internet IAEA GNIP (Global Network of Isotopes in

11 Precipitation) data were available for thorough subregime separation and consequent evaluation of groundwater genesis. For past interpretation, δ 18 O values were plotted against discharges (Fig. 4). In the spring Tri mlynky with the dolomitic aquifer in the recharge area, heavier oxygen isotopes in water were found with increasing discharge, while in spring Vítek (more karstified limestone recharge area) the increased volume of discharged groundwater was more depleted in δ 18 O (Malík et al. 1992). Twenty years after completion of this intensive hydrogeological investigation, digital processing of discharge curves and springs discharge separation into subregimes enabled more thorough additional research on groundwater genesis consequences. Various stages of the spring's recession curve - flatter parts for groundwater draining small fissures, steeper parts for groundwater circulating in more opened fissures or karst conduits could be described by superposition of series of equations. While basic laminar subregime with α 1 values 1 to day -1 could be linked to all springs, the 2 nd laminar subregime (α 2 values 9 to day -1 ) was recognized at two springs (Vítek and Stužková) and the turbulent flow subregime, marking the presence of flow in karst channels was found in three of them (except Tri mlynky spring, see Tab. 4 and Figs. 4 and 5). The main principle of hydrograph separation into subregimes was a presumption, that the discharge of an aquifer depends on the level of its groundwater saturation, and that the same discharge reflects the same groundwater saturation level. The hydrograph separation itself was based on iterative solution of exponential and linear equations sequence. Groundwater, discharging at individual springs, was considered to be a mixture of various groundwater types; maybe originated as different subregimes, each of which can be characterised by δ 18 O (SMOW) values. Proportional representation of individual subregimes discharge on the total discharge (in %) then lead to of both δ 18 O and groundwater temperature forecast for 100 % representation of each subregime. In the case of the Vítek spring, the water outflowing in 2 nd laminar subregime seems to be both more depleted in δ 18 O ( %), and colder in temperature values (9.66 C), in comparison to the 1 st laminar baseflow ( % / C). Turbulent subregimes in springs Vítek and Spod javora seem to be unrealistically exaggerated in calculated water temperatures, but maybe suggest on contact with the uppermost part of the aquifer affected by sun radiation. In the case of spring Spod javora turbulent subregime, extremely heavy content of oxygen isotopes (-5.24 %) was calculated. All the basic (1 st ) laminar subregimes of springs in the Brezovské Karpaty Mts. seem to have similar oxygen isotope composition of water ( in average), not very different from the overall average ( ) due to substantial representation of the basic (1 st laminar) regime on total discharge (83.6 % in all springs average). In some cases, quantitative regime was found as uninterpertable using recession curves analyses, due to improper records in the past. The discharge of springs at the time period of investigation ( ) was monitored weekly (each Wednesday) by an observer, and values reported by Slovak Hydrometerorological Institute were not in agreement with the observed one during the samplings. In all cases, directly observed discharges were used for determining proportions of subregimes. Obtained results are based only on sparsely populated datasets and manual discharge records, but seem to represent a perspective method for future interpretations. In future, also groundwater chemical properties can be processed in the same way. REFERENCES Began, A., Hanáček, J., Mello, J., & J. Salaj, 1984: Geologická mapa Myjavskej pahorkatiny, Brezovských a Čachtických Karpát. SGÚ, GÚDŠ, Slovenská kartografia, Bratislava. Map sheet 1 : , Bratislava Bella, P., Hlaváčová, I., & P. Holúbek, (eds.) 2007: Zoznam jaskýň Slovenskej republiky. Slovenské múzeum ochrany prírody a jaskyniarstva, Správa slovenských jaskýň, Slovenská speleologická spoločnosť, ISBN , 364 pp., Liptovský Mikuláš Boussinesq, J., 1877: Essai sur la theories des eax courantes. Memoires presentes par divers savants a l Academie des Sciences de l Institut National de France, Tome XXIII, No. 1

12 Goldscheider, N., & D. Drew, (eds.) 2007: Methods in Karst Hydrogeology. International contributions to hydrogeology, 26. International Association of Hydrogeologists, Taylor & Francis, 264 pp., Kullman, E., 1983: Režim podzemných vôd s turbulentným prúdením v puklinovo krasovom horninovom prostredí. Geologické práce, 79, Geologický ústav Dionýza Štúra, Bratislava, Kullman, E., 1990: Krasovo puklinové vody. Karst-fissure waters. Geologický ústav Dionýza Štúra, 184 pp., Bratislava Kullman, E. 2000: Nové metodické prístupy k riešeniu ochrany a ochranných pásiem zdrojov podzemných vôd v horninových prostrediach s krasovo puklinovou priepustnosťou. Podzemná voda, VI., 2/2000, Slovenská asociácia hydrogeológov, Bratislava, Maillet, E., 1905: Essais d Hydraulique Souteeraine et Fluviale. Hermann Paris, 218 p. Malík, P., Kullman, E. & K. Vrana, 1992: Hydrogeológia karbonátov mezozoika Brezovských Karpát. Západné Karpaty, séria hydrogeológia a inžinierska geológia, No.10, Geologický ústav Dionýza Štúra Bratislava, Malík, P., Michalko, J. & S. Rapant, 1993: Štruktúrno-hydrogeologická analýza karbonátov triasu krížňanského príkrovu vo Veľkej Fatre, Manuscript Archive of the Geofond Branch of the State Geological Institute of Dionýz Štúr, Arch. No , 277 pp., Bratislava Malík, P., 2007: Assessment of regional karstification degree and groundwater sensitivity to pollution using hydrograph analysis in the Velka Fatra Mts., Slovakia. Water Resources and Environmental Problems in Karst. Environmental Geology (2007), 51, Salaj, J., Began, A., Hanáček, J., Mello, J., Kullman, E., Čechová, A., & P. Šucha, 1987: Vysvetlivky ku geologickej mape Myjavskej pahorkatiny, Brezovských a Čachtických Karpát. Geologický ústav Dionýza Štúra, Veda vydavateľstvo SAV, 183 pp., Bratislava

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