Advertisement

Environmental Science and Pollution Research

, Volume 26, Issue 7, pp 7115–7122 | Cite as

Origin and behavior of radionuclides in sediment core: a case study of the sediments collected from man-made reservoirs located in the past mining region in Central Slovakia

  • Katarzyna SzarlowiczEmail author
  • Marcin Stobinski
  • Ladislav Hamerlik
  • Peter Bitusik
Open Access
Research Article
  • 597 Downloads

Abstract

The analyzed sediments were taken from the man-made reservoirs (Velka Richnava, Rozgrund and Vindsachta) located in an area intensively mined for polymetallic ores since the end of the eleventh century (Banska Stiavnica region, Central Europe). The aims of this study were to determine the radioactivity of natural (226Ra, 228Th, 210Pb) and artificial (137Cs and 241Am) radionuclides, compare the radionuclides’ distribution, and indicate the correlation of radioisotopes and their origin related to sediment properties. Two analytical techniques were used. 228Th, 226Ra, 241Am, and 137Cs were measured by means of gamma spectrometry and 210Pb was determined by its daughter radionuclide 210Po using alpha spectrometry. The results showed that the highest mean level of 226Ra (42.6 Bq·kg−1), 228Th (49.7 Bq·kg−1) and 210Pb (75.2 Bq·kg−1) was in the sediments collected from Rozgrund. The radioactivity of 137Cs and 241Am were present at a higher level in the layer related to Chernobyl (1986) accident and nuclear weapon test (1950/1960). The distribution of natural radionuclides was quite similar in all reservoirs. Chemometric analysis confirmed the radionuclides’ origin and correlation between the analyzed parameters.

Keywords

Radionuclides Sediments Artificial reservoirs Gamma spectrometry Chemometric analysis Pollution 

Introduction

Radioactivity is a natural part of the environment. Radionuclides are present in every environmental component (air, water, sediments, soils, plants, or animals). The naturally occurring radioisotopes can be divided into three groups, depending on their origin. Primordial radionuclides have existed since the Earth was formed, around 4.6 × 109 years ago, while cosmogenic are produced in nuclear reactions between and the constituents/elements present in the atmosphere or the surface of the earth. The third group contains the radionuclides from the radioactive decay series (uranium–radium (i.e., –226Ra–222Rn–218Po–214Pb–214Bi–214Po–210Pb–), uranium–actinium (i.e., –231Th–227Ac–223Ra–215Po–211Bi–207Pb–), and thorium (i.e., –228Ra–228Ac –228Th–220Rn–212Pb–212Bi–208Tl–)) (Isaksson and Raaf 2016). All minerals and raw materials contain radionuclides of natural origin. Certain industrial activities (coal industry, metal mining, smelting, mineral sands, etc.) can give rise to significantly enhanced radiation exposures. Material giving rise to these enhanced exposures has become known as naturally occurring radioactive material (NORM). Mining and processing of metal ores may also generate large quantities of NORM waste. In iron smelting, radioactivity can even reach about 100 kBq∙kg−1 for 210Pb and 210Po in dust (Cooper 2003).

However, with the discovery of neutrons by James Chadwick in 1932, a number of radionuclides of non-natural origin began to be created (Keller et al. 2011). Uncontrolled release of artificial radionuclides is a big problem for the environment safety, due to disturbance of the natural background of ionizing radiation. The dominant sources of anthropogenic radioactivity are accidental releases such as Chernobyl (1986) and global weapons testing 1950/1960 (maximum deposits in 1963). In fact, large areas of Europe taking into account all environmental components were contaminated (Hodge et al. 1996; UNSCEAR 2000; Evangeliou et al. 2013). From radio-ecological point of view, the most important elements are the long-lived radionuclides, i.e., 137Cs (T1/2 = 30.05 y) or 90Sr (T1/2 = 28.8 y). Nowadays, attention should be also paid to 241Am (T1/2 = 432.6 y), the element which is formed exclusively as a result of nuclear fission processes as a daughter nuclide of plutonium 241Pu (Appleby et al. 1991; DOE 2000; Lehto and Hou 2011). All natural or artificial radionuclides can be present in sediments. Sediments can be treated as a repository for different kinds of contaminants including radionuclides (Skwarzec 1995; Appleby 2001; Szarlowicz et al. 2018). In this work, we would like to present the level of 137Cs, 241Am, 226Ra, 210Pb, and 228Th in the sediment samples taken from the man-made reservoirs situated in the Stiavnicke vrchy Mountains in the inner belt of the West Carpathians. The mountain range was formed during several stages of andesitic and rhyolitic volcanism in the Middle and Late Miocene (Chernyshev et al. 2013).

Therefore, the adjacent area around the town Banska Stiavnica is rich with iron and polymetallic ores containing lead, zinc, copper, gold, and silver (Konečný 1971). This region, together with some other sites in the Central Slovakia, occupied a dominant position among the medieval mining regions in Europe. History of mining in Banska Stiavnica surroundings has been recorded since the end of the eleventh century to the turn of the twentieth century, although traces of the mining have been documented from the Bronze Age (Labuda 2016; Lichner 2002).

The surveyed reservoirs have been a part of the hydro-energetic system that was completed during the biggest expansion of mining between the beginning of the eighteenth and the first half of the nineteenth century. Water from this system provided energy for operating of mining machines, ore cleaning facilities, and smelting works (Novák 1977). The reservoirs and other technical monuments situated in a unique, man-modified landscape were inscribed in the World Cultural and Natural Heritage List UNESCO in 1993.

The previous multi-proxy palaeolimnological studies (Bitušík et al. 2018) have documented a potential of the sediments for the reconstructions of an ontogeny of these reservoirs and for expanding the current knowledge of changes in mining landscapes that are rarely described in historical documents.

The main focus of this study was to compare distribution, correlation of radioisotopes, and their origin related to sediments properties for three reservoirs Velka Richnava, Rozgrund, and Vindsachta. To do this, basic chemometric tools were used.

Material and method

Study sites

The surveyed reservoirs are located in an open landscape with mosaic of mixed forests, grasslands, and settlements. While Velka Richnava (RICH) and Vindsachta (VIND) belong to the same reservoir group and were interconnected via gallery, Rozgrund (ROZ) is about 20 km away. The bedrock of VIND and RICH and their surroundings consists of pyroxene and amphibole-pyroxene andesite with accessory biotite, quartz, and garnet altered by successive hydrothermal activity. The surroundings of ROZ are more heterogeneous and consist of mineralogical varieties of andesite and diorite and hydrothermally altered veins. Deluvial deposits, mostly loamy stony and stony screes, cover the bedrock of all reservoirs (Konečný et al. 1998).

While ROZ has served as a source of drinking water with protected watershed since the second half of the 1920s, the surroundings of RICH and VIND are partially urbanized. The function of both reservoirs is primarily to support recreation, such as swimming, boating, and angling. A more detailed description of the studied sites is given in Table 1.
Table 1

Characteristics of the surveyed reservoirs

Reservoir

Velka Richnava

Vindsachta

Rozgrund

Coordinates

N 48°25′37″

E 18°50′46″

N 48°26′03″

E 18°51′22″

N 48°28′39″

E 18°52′32″

Year of building

1740

1715

1743

Altitude [m a.s.l.]

725

688

703

Area [m2]

82,830

46,540

54,350

Max depth [m]

19.5

12.7

20.9

Volume [m3]

~ 666,000

~ 285,000

~ 575,000

Sampling

The sediment core samples were collected using the UWITEC Niederreiter 60 (Ø 6.0 cm) hydraulic coring system. From each reservoir, two sediment cores were obtained (core length RICH—1.84, 1.10 m; ROZ—4.20, 3.53 m; and VIND—1.2, 1.03 m). The core samples were divided into 1-cm sections. They were packed into plastic bags and stored in a refrigerator for later analysis. Only chosen samples from the longer core were analyzed.

Preparation and measurements

The samples were dried in a room temperature, grinded in a mortar, and packed into the calibrated flat round vessels (volume 1.5 cm3, 2.7 cm internal diameter). The radioisotope determination of the samples was carried out by two different techniques. For gamma radionuclides, high-resolution gamma spectrometry with HPGe detector (Canberra model BE3830 with carbon composite window and relative efficiency 34%) was used. The radioactivity of 137Cs and 241Am was found by photo peaks at 661.6 keV and 59.5 keV respectively. The photo peaks used for 226Ra came from 214Pb (351.9 keV, 295.2 keV) and 214Bi (1764.5 keV, 1120.3 keV, 609.3 keV). The 228Th was determined by gamma lines from 212Pb (238.6 keV), 212Bi (727.3 keV), and 208Tl (2614.5 keV, 583.1 keV).

210Pb radioactivity was determined by means of its daughter alpha radionuclide 210Po. Based on the amount of the taken sediment, the alpha spectrometry is the most sensitive measurement method. The radiochemical procedure consisted of microwave sample (0.2 g) digestion with concentrated nitric and hydrochloric acids (Anton Paar Multiwave Pro), evaporation to dryness and dissolving of the residue in 2 mol dm−3 HCl, and the source preparation in the presence of hydroxylamine hydrochloride and sodium tri-citrate. 208Po was added to every sample in order to calculate the efficiency of the procedure. 210Pb was calculated after two depositions of polonium in time of about 6 months (Szarlowicz et al. 2013). Sources were measured 3–5 days. An Alpha spectrometer model 7401 was used. All spectra were analyzed using Genie—2000 software. In both cases, to check the method, the reference materials from IAEA (International Atomic Energy Agency, IAEA-447, IAEA-RGU-1, IAEA-RGTh-1) were measured. In alpha spectrometry, the blank solution also was measured. As for gamma, the radionuclide background was checked monthly.

Organic matter content

The organic matter content was determined as loss-on-ignition (LOI) and expressed as the percentage weight loss after combustion at 550 °C for 4 h (Heiri et al. 2001).

Statistical data analysis

To distinguish relevant information out of the obtained data, the data matrix consisting of all analyzed features of all samples was analyzed statistically (separately for each reservoir). Chemometric tools, i.e., cluster analysis (CA) and principal components analysis (PCA), were used (using Statistica 10 and Stagraphics Centurion software).

Results and discussion

The activity of the natural radionuclide and other parameters are shown in Table 2. The uncertainty of the radioactivity measurements was not higher than 20%.
Table 2

Natural radionuclides’ concentration and basic data for the samples from the studied reservoirs

 

VIND (n = 13)

RICH (n = 13)

ROZ (n = 10)

Average

Minimum

Maximum

Average

Minimum

Maximum

Average

Minimum

Maximum

228Th [Bq·kg−1]

38.9

29.0

64.5

35.5

27.1

50.4

49.7

40.2

68.1

226Ra [Bq·kg−1]

37.8

27.4

55.5

33.5

26.8

44.4

42.6

28.5

68.5

210Pb [Bq·kg−1]

62.1

21.0

226.0

35.5

15.3

251.0

75.2

29.1

278.0

Organic matter [%]

10.5

7.4

15.2

7.1

3.8

12.4

9.5

7.1

13.3

Density [g cm−3]

1.1

0.8

1.3

0.9

0.5

1.3

0.7

0.5

1.0

Depth [cm]

45

2

103

86

1

171

136

3

321

It was found that the levels of average radioactivity of 226Ra and 228Th in the RICH and VIND reservoirs were similar. In ROZ, the highest radioactivity of 226Ra was observed. The same situation was applied to the levels of 228Th with the highest average level for ROZ. The distribution of 226Ra and 228Th within the sediment core showed a very similar pattern in all three lakes. The distribution was rather regular, only minor deviations were observed. The levels of radioactivity were connected with mineralogical composition of the sediments as coarse grained sand and gravel in the older layers were replaced by sand, silt, and clay in the younger ones (Bitušík et al. 2018). So, the activity concentration can show local deviations from that of 238U or 232Th (mother radionuclide) due to weathering and other environmental factors.

The results of 210Pb radioactivity for all three lakes are also presented in Table 2. The 210Pb radioactivity in the top layers was almost on the same level, going deeper the values decreased exponentially (see Chamutiova et.al 2018). The tendency of the lead radioactivity changes in RICH and ROZ indicate similarity of the sediments’ deposition processes. Besides, there were also visible some small irregularities along the sediment’s core. A little different situation was observed for VIND; here, a regular decrease of radioactivity was observed. The obtained results were used to determine the age of sediments using the 210Pb method. In the RICH, the 171-cm long sediment core was deposited over the last ca. 174 years. The sediment core from ROZ represents the sediments from the last 191 years. The 82 cm in the VIND started to deposit at the beginning of the nineteenth century. The 210Pb and 137Cs geochronology results have been published (Bitušík et al. 2018, Chamutiová et al. 2018).

Artificial radionuclides were also identified. In some layers, it was possible to perform quantitative determination but in the other, only qualitative information was obtained. In some of the samples (in the majority of ROZ), the 137Cs radioactivity was below the limit of detection. In ROZ, the 137Cs was only determined in the uppermost layer. The value was about 128.0 ± 4.5 Bq·kg−1. The 137Cs radioactivity in the VIND reservoir was present in the 26 cm of the core in the range from 41.5 ± 3.8 to 202.0 ± 6.3 Bq·kg−1. Regarding 137Cs radioactivity in RICH, it was identified in the samples 0–1 cm (540 ± 7 Bq·kg−1), 10–11 cm (11 ± 3 Bq·kg−1), 40–41, and 50–51 cm (< 6 Bq·kg−1).

In the VIND reservoir, 241Am was well defined. The presence of 241Am was about 5.4 ± 1.2 Bq·kg−1 and it was observed from 1 to 32 cm. The highest level of 241Am was found in the 20–21 cm (1965) and 31–32 cm (1953) layers. In RICH analyzed spectra, only counts from americium at 50–51 cm (1956) were observed, but the number of counts was too small to quantify them. Regarding ROZ, there were also some counts dedicated to the uppermost layer and also to 110–111 (1962). The year in brackets represents the year ascribed to the layer determined by 210Pb dating.

Statistical correlation analysis was performed in order to evaluate the factors having influence on the radionuclides concentrations. In all three reservoirs, the correlation showed a very strong correlation between the analyzed parameters. The correlation coefficient according to Spearman rank-order was done. The best correlation was found in VIND. The values of the correlation coefficients are presented in Table 3. A positive correlation of 137Cs with 241Am, 210Pb, and organic matter was observed and a negative one with depth. 137Cs and 241Am have the same anthropological origin. They were present only in the younger layers. To compare the layers, the graphical presentation of CA with Ward’s method and Euclidean distance was done separately for each reservoir. All results were standardized prior to chemometric analysis. Figure 1 represents the results for RICH.
Table 3

Spearman’s rank-order correlation for the VIND lake. Marked correlation coefficients are significant with p < 0.50

 

Organic matter

Density

137Cs

228Th

226Ra

241Am

210Pb

Depth

− 0.857

0.989

− 0.839

− 0.140

− 0.187

− 0.794

− 0.990

Organic matter

 

− 0.857

0.748

0.179

0.024

0.686

0.819

Density

  

− 0.830

− 0.096

− 0.140

− 0.806

− 0.976

137Cs

   

0.091

0.343

0.701

0.807

228Th

    

0.564

0.080

0.135

226Ra

     

0.179

0.150

241Am

      

0.768

Fig. 1

Cluster analysis for the RICH lake. Dendrogram aglomerated with Ward’s method, Euclidean distance

Evidently, the first layer was totally different from the others. Considering the remaining layers, two main clusters could be distinguished. The first cluster (green line) represented in the majority of the samples at the depth above 100 cm (up to 1933), while the second (red line) contained the shallower layers (older samples up to ca 1840). The samples 21 and 121 were the exceptions. It can result from the sediments’ composition. Very-low level of organic matter content in the sample 21 can be correlated with high mineralization as a result of oxygen presence caused by drainage of the reservoir. On contrary, the sample 121 was found in the cluster with high content of organic matter caused by erosive contact (Bitušík et al. 2018).

In Figs. 2 and 3, the dendrograms for ROZ and VIND are presented. Here, three main clusters could be distinguished. In both reservoirs, the first cluster (black line) represented the youngest samples (ROZ 2013–1996 and VIND 2013–1987) and these were sediments with characteristic totally different from the others. In the cluster marked with green, sediments formed in the years 1936–1973 for VIND and 1940–1973 for ROZ are gathered. The third cluster (red line) consists of the oldest sediments layers (up to 1816—VIND and 1825—ROZ, respectively).
Fig. 2

Cluster analysis for the ROZ lake. Dendrogram aglomerated with Ward’s method, Euclidean distance

Fig. 3

Cluster analysis for the VIND lake. Dendrogram aglomerated with Ward’s method, Euclidean distance

Regarding the origin of the radionuclides, the PCA makes the situation quite clear. Based on the PCA analysis with Kaisser’s criterion, it was found that 82.8% (ROZ) and 85.9% (VIND) of the variability contained in the considered set of data can be described using the two principal components. In Figs. 4 and 5, it is shown that the first principal component was positively correlated with depth and density. Negative correlation was ascribed to the organic matter content, 137Cs and 210Pb. 228Th and 226Ra were described by the second principal component.
Fig. 4

The biplot with projection of the variables and cases onto the plane of the first two principal components for the ROZ lake

Fig. 5

The biplot with projection of the variables and cases onto the plane of the first two principal components for the VIND lake

In RICH, three principal components were needed for the description of the component relationship in the sediments (Fig. 6). They represent 82.5% of the variance.
Fig. 6

The biplot with projection of the variables and cases onto the plane of the first three principal components for the RICH lake

Additionally, factor analysis (PCA factoring) with varimax rotation was used. In Table 4, the factor loadings matrix after varimax rotation is presented. Vari factor-1 was positively correlated with depth and density and negatively with the organic matter content and 228Th. 137Cs and 210Pb were negatively correlated with vari factor-2, and vari factor-3 represents 226Ra.
Table 4

Factor loading matrix after varimax rotation for the RICH lake

 

Vari factor—1

Vari factor—2

Vari factor—3

Depth

0.758

0.317

0.122

Organic matter

− 0.764

− 0.388

− 0.310

Density

0.814

0.356

0.049

137Cs

− 0.173

− 0.970

− 0.091

228Th

− 0.710

0.008

0.153

226Ra

0.079

0.064

0.978

210Pb

− 0.255

− 0.958

− 0.025

The Principal Component analysis revealed that the activities of 137Cs and 210Pb, as well as the concentration of organic matter in the sediments cores, are strongly and positively correlated, simultaneously being negatively correlated with the profile depth and sediments’ density. It can be attributed to the fact that both anthropogenic 137Cs and natural 210Pb (mainly its unsupported component) were delivered to the reservoir area in the result of dry and wet deposition (long distance character). It can also be observed in the analysis of the correlation matrix (Table 3). Those radionuclides reveal strong affinity to organic matter, so the higher content of organic matter, the higher activity of radionuclides (Bolsunovsky et al. 2005; Szarłowicz et al. 2011, Stobinski et al. 2014). Going deeper into the profile, the content of organic matter decreases which is accompanied by the increase of mineral content and density of the examined sediments. 228Th and 226Ra (natural radionuclides) are formed in situ being the component of mother rock, soil, or particulate matter and were constantly delivered from the surrounding area to the reservoirs (local character).

Conclusions

For the first time, in respect to the radionuclides in the selected reservoirs, such research was proposed, performed, and discussed. The following can be concluded:
  1. 1.

    the radioactivity levels of 226Ra and 228Th are comparable to those present in the Earth’s crust and in the sediments taken from stream and river sediments in Central Slovakia region (UNSCEAR 2000; Cabáneková and Melicherová 2015);

     
  2. 2.

    the distribution of 210Pb can explain the process of sediment’s deposition;

     
  3. 3.

    in none of the sediments’ cores, there was no distinct 137Cs maximum peak determined. However, relating to the time scale (based on 210Pb dating), elevated levels of the radionuclide were found;

     
  4. 4.

    it was confirmed that 241Am is also a good time marker, the presence of maximum in sediment core verified it. It can be used as an additional confirmation of the date especially in relation to nuclear weapon test;

     
  5. 5.

    despite the different location and functions of the reservoirs (RICH and VIND—recreation, ROZ—a drinking water reservoir), the sediments contain radionuclides at a quite similar level. Small differences are mainly related to the distribution of the artificial radionuclides and composition of the sediments;

     
  6. 6.

    it is assumed that both 137Cs and 241Am were at the measurable level in VIND due to the highest content of organic matter. Besides, it suggests that the function of the reservoir has no influence on radionuclides distribution;

     
  7. 7.

    Summarizing, radiochemical analysis of the sediments together with statistical approach provides valuable information about the origin and behavior of radionuclides in the environment. Chemometric analysis confirmed the radionuclides origin and correlation between the parameters. The presented chemometric analysis suggests that the applied methodology might be useful in the analyses of the date deposition of the layers in other reservoirs or lakes, respectively in the region.

     

Notes

References

  1. Appleby PG (2001) Chronostratigraphic techniques in recent sediments. In: Last WM, Smol JP (eds) Tracking environmental change using lake sediments Volume 1: basin analysis, coring, and chronological techniques. Kluwer Academic Publishers, Dordrecht, pp 171–203Google Scholar
  2. Appleby PG, Richardson N, Nolan PJ (1991) 241Am dating of lake sediments. Hydrobiologia 214:35–42.  https://doi.org/10.1007/BF00050929 CrossRefGoogle Scholar
  3. Bitušík P, Trnková K, Chamutiová T, Sochuliaková L, Stoklasa J, Pipík R, Szarlowicz K, Szacilowski G, Thomková K, Šporka F, Starek D, Šurka J, Milovský R, Hamerlík L (2018) Tracking human impact in a mining landscape using lake sediments: a multi-proxy palaeolimnological study. Palaeogeogr Palaeoclimatol Palaeoecol 504:23–33.  https://doi.org/10.1016/j.palaeo.2018.04.021 CrossRefGoogle Scholar
  4. Bolsunovsky A, Zotina T, Bondareva L (2005) Accumulation and release of 241Am by a macrophyte of the Yenisei River (Elodea canadensis). J Environ Radioact 81:33–46CrossRefGoogle Scholar
  5. Cabáneková H and Melicherová T (2015) Správa o radiačnej situácii na území Slovenskej republiky za rok 2015. Radiačná situácia v SR v roku 2015 1–40 (In Slovak)Google Scholar
  6. Chamutiová T, Hamerlík L, Szarlowicz K et al (2018) The historical development of three man-made reservoirs in a mining region: a story told by subfossil chironomids. J Limnol 77(s1):220–229Google Scholar
  7. Chernyshev IV, Konečný V, Lexa J, Kovalenker VA, Jeleň S, Lebedev VA, Goltsman YV (2013) K-Ar and Rb-Sr geochronology and evolution of the Štiavnica Stratovolcano (Central Slovakia). Geol Carpath 64:327–351CrossRefGoogle Scholar
  8. Cooper MB (2003) Naturally occurring radioactive materials (NORM) in Australian industries - review of current inventories and future generationGoogle Scholar
  9. DOE (U.S. Department of Energy) (2000) Buried transuranic-contaminated waste information for U.S. Department of Energy Facilities. Office of Environmental Management, Washington, D.CGoogle Scholar
  10. Evangeliou N, Balkanski Y, Cozic A, Møller AP (2013) Simulations of the transport and deposition of 137Cs over Europe after the Chernobyl Nuclear Power Plant accident: influence of varying emission-altitude and model horizontal and vertical resolution. Atmos Chem Phys 13:7183–7198.  https://doi.org/10.5194/acp-13-7183-2013 CrossRefGoogle Scholar
  11. Heiri O, Lotter AF, Lemcke G (2001) Loss on ignition as a method for estimating organic and carbonate content in sediments: reproducibility and comparability of results. J Paleolimnol 25:101–110.  https://doi.org/10.1023/A:1008119611481 CrossRefGoogle Scholar
  12. Hodge V, Smith C, Whiting J (1996) Radiocesium and plutonium: still fixed together in background soils after more than thirty years. Chemosphere 32:2067–2075CrossRefGoogle Scholar
  13. Isaksson M, Raaf CL (2016) Environmental radioactivity and emergency preparedness. CRC Press Taylor and Francis Group, Boca RatonCrossRefGoogle Scholar
  14. Keller C, Wolf W, Shani J (2011) Radionuclides. 2. Radioactive elements and artificial radionuclides. In Ullmann’s encyclopedia of industrial chemistry.  https://doi.org/10.1002/14356007.o22_o15
  15. Konečný V (1971) Evolutionary stages of the Banská Stiavnica caldera and its post-volcanic structures. Bull Volcanol 35(1):95–116CrossRefGoogle Scholar
  16. Konečný V, Lexa J, Halouzka R et al (1998) Explanatory notes to the geological map of Štiavnické vrchy and Pohronský Inovec mountain ranges (Štiavnica Stratovolcano). Geological Survey of Slovak Republic, Bratislava (In Slovak with English summary)Google Scholar
  17. Labuda J (2016) Glanzengerg in Banská Štiavnica. Archeological survey of an abandoned town. Slovenské banské múzeum, Banská Štiavnica (In Slovak with English summary).Google Scholar
  18. Lehto J, Hou X (2011) Chemistry and analysis of radionuclides. Wiley-vch Verlag Gmbh&Co, WeinheimGoogle Scholar
  19. Lichner M (2002) Banská Štiavnica. The testimony of time. Studio Harmony, Banská Bystrica (In Slovak)Google Scholar
  20. Novák J (1977) The water management system in Banská Štriavnica Ore District and its function in the past. Proceedings of Slovak Mining Museum in Banská Štiavnica 8:109–141 (In Slovak with English summary)Google Scholar
  21. Skwarzec B (1995) Polonium uranium and plutonium in the ecosystem of southern Baltic. PAN, Sopot (In Polish)Google Scholar
  22. Stobinski M, Szarlowicz K, Reczynski W, Kubica B (2014) The evaluation of 137Cs radioactivities in soils taken from the Babia Góra National Park. J Radioanal Nucl Chem 299(1):631–635.  https://doi.org/10.1007/s10967-013-2809-z CrossRefGoogle Scholar
  23. Szarłowicz K, Reczyński W, Gołaś J et al (2011) Sorption of 137Cs and Pb on sediment samples from a drinking water reservoir. Pol J Environ Stud 20(5):1305–1312Google Scholar
  24. Szarlowicz K, Reczynski W, Misiak R, Kubica B (2013) Radionuclides and heavy metal concentrations as complementary tools for studying the impact of industrialization on the environment. J Radioanal Nucl Chem 298(2):1323–1333.  https://doi.org/10.1007/s10967-013-2548-1 CrossRefGoogle Scholar
  25. Szarlowicz K, Reczynski W, Czajka A, Spyt B, Szacilowski G (2018) Comprehensive study of the mountainous lake sediments in relation to natural and anthropogenic processes and time (Mały Staw Lake, Poland). Environ Sci Pollut R 25:3335–3347.  https://doi.org/10.1007/s11356-017-0711-x CrossRefGoogle Scholar
  26. United Nations Scientific Committee on the Effects of Atomic Radiation (2000) Sources and effects of ionizing radiation, volume I: Sources. UNSCEAR 2000 Report to the General Assembly, with scientific annexesGoogle Scholar

Copyright information

© The Author(s) 2019

Open Access This article is distributed under the terms of the Creative Commons Attribution 4.0 International License (http://creativecommons.org/licenses/by/4.0/), which permits unrestricted use, distribution, and reproduction in any medium, provided you give appropriate credit to the original author(s) and the source, provide a link to the Creative Commons license, and indicate if changes were made.

Authors and Affiliations

  1. 1.Faculty of Energy and FuelsAGH University of Science and TechnologyKrakowPoland
  2. 2.Faculty of Natural SciencesMatej Bel UniversityBanská BystricaSlovakia
  3. 3.Institute of Geological SciencesPolish Academy of SciencesWarsawPoland

Personalised recommendations