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Sedimentological and geochemical traces of metallurgical activity in the Świślina River valley (central Poland) at the Doły Biskupie site

Published online by Cambridge University Press:  03 January 2024

Paweł Przepióra Open the ORCID record for Paweł Przepióra [Opens in a new window]  and
Tomasz Kalicki Open the ORCID record for Tomasz Kalicki [Opens in a new window]
Paweł Przepióra*
Affiliation:
Department of Geomorphology and Geoarchaeology, Institute of Geography and Environmental Sciences, Jan Kochanowski University in Kielce, 25-406 Kielce, Poland
Tomasz Kalicki*
Affiliation:
Department of Geomorphology and Geoarchaeology, Institute of Geography and Environmental Sciences, Jan Kochanowski University in Kielce, 25-406 Kielce, Poland
*
Corresponding authors: P. Przepióra; Email: [email protected]; T. Kalicki; Email: [email protected]
Corresponding authors: P. Przepióra; Email: [email protected]; T. Kalicki; Email: [email protected]
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Abstract

Prehistoric and historic iron metallurgy in the Holy Cross Mountains in central Poland developed along with human Przeworsk Culture activity (during the Roman period) and within the boundaries of the Old-Polish Industrial District (OPID) during the Middle Ages and during recent centuries. At the Świślina catchment, there are many archaeological sites showing intense prehistoric metallurgical activity. The later medieval and modern iron industry was significantly smaller. At the Doły Biskupie site, slags and microscopic iron spherules (hammerscales) were found in alluvia. The microscopic spherules separation method (MSS) enabled analysis of these small artefacts created during iron ore smelting and forging. Iron spherules were detected in floodplain sediments, which are characterized by increased content of trace elements. The presence of these artefacts in shallow sediment layers in the confluence section of the river may be an indicator of archaeologically confirmed prehistoric metallurgical activity in the catchment area. Study of these residues enabled an attempt to reconstruct the river valley environment during the prehistoric and historical period. The MSS method can be used to detect iron spherules in alluvia in other river catchments, confirming the presence of yet-undiscovered bloomery sites.

Keywords

Micro- and macroslagsHammerscalesOld-Polish Industrial DistrictBloomeriesPrehistoric and historical metallurgyŚwiślina River valleyHolly Cross Mountains
Type
Research Article
Information
Quaternary Research , Volume 119 , May 2024 , pp. 1 - 11
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Copyright
Copyright © The Author(s), 2024. Published by Cambridge University Press on behalf of Quaternary Research Center

INTRODUCTION

Research on the occurrence of traces of human activity in landforms and sediments has been undertaken for many years. Soil erosion products were carried to the main river valleys, forming so-called cultural sediment (Natermann, Reference Natermann1941), flood, bottom, anthropogenic muds (e.g., Klimaszewski, Reference Klimaszewski1948; Poser and Tricard, Reference Poser and Tricard1950; Mensching, Reference Mensching1951a, Reference Mensching1951b, Reference Mensching1957; Reichelt, Reference Reichelt1953; Zandstra, Reference Zandstra1954; Hempel, Reference Hempel1956, Reference Hempel and Richter1976; Klatka, Reference Klatka1958; Lüttig, Reference Lüttig1960; Jäger, Reference Jäger1962; Mäckel, Reference Mäckel1969; Huckriede, Reference Huckriede1971; Schirmer, Reference Schirmer1973; Linke, Reference Linke1976; Loźek, Reference Loźek1976; Modderman, Reference Modderman1976), or agricultural muds (Rutkowski et al., Reference Rutkowski, Alexandrowicz and Pazdur1988; Rutkowski, Reference Rutkowski1991), a sediment typical for the Subboreal and especially for the Subatlantic. Further research results from various areas proved, however, that these muds were deposited throughout the late glacial and Holocene, although at a different rate (Kalicki, Reference Kalicki2006). Many authors, however, still closely associate the appearance and sedimentation of these muds with an anthropogenic factor (e.g., Klimek, Reference Klimek1988, Reference Klimek, Howard, Macklin and Passmore2003; Lipps, Reference Lipps1988; Hiller et al., Reference Hiller, Litt and Eissmann1991; Pastre et al., Reference Pastre, Cecchini, Dietrich, Fontugne, Gauthier, Kuzucuoglu, Leroyer and Limondin1991; Litt, Reference Litt and Frenzel1992; Brown, Keough, Reference Brown and Keough1992a, Reference Brown, Keough, Needham and Macklin1992b; Alexandrowicz, Reference Alexandrowicz1996), which undoubtedly had a strong influence from the Middle Ages (e.g., Schirmer, Reference Schirmer and Hagedorn1995; Klimek, Reference Klimek and Kostrzewski1996; Houben, Reference Houben2003) and initiated such deposition in small mountain catchments in the last few centuries (e.g., Hong, Reference Hong1995; Mäckel and Zollinger, Reference Mäckel, Zollinger and Hagedorn1995; Klimek et al., Reference Klimek, Malik, Owczarek and Zygmunt2003; Houbrechts et al., Reference Houbrechts, Petit, Kalicki and Michalczyk2004; Kukulak, Reference Kukulak2004).

Research in the Doły Biskupie area has shown that this type of anthropogenic sediment formed a terrace (11–9 m above river level [m arl]) and a floodplain (5.5–4.5 m arl) that accumulated during the smelting activity period, which is confirmed by slag remnants found in alluvia (Klatka, Reference Klatka1958). These slags can be connected with the prehistoric (Roman period) (Radwan, Reference Radwan1963; Bielenin, Reference Bielenin1992; Orzechowski, Reference Orzechowski2007) or even the medieval metallurgy activity operating within the Old-Polish Industrial District (OPID) area. These remnants are mostly bloomery slags that were discovered throughout the entire catchment area. Intensive archaeological research aimed at analysing these artefacts was carried out in the second half of the twentieth century. However, there is a lack of any wider analysis of the human–environment context within this subject. Using mainly aerial photography and environmental intelligence, more bloomery sites were found. The prehistoric iron ore excavation source theory has not been fully explained. It is suggested that the shallow iron ore was obtained from limonite, which was found in karst depressions or in other lowlands (Janiec and Kardyś, Reference Janiec, Kardyś, Dąbrowski and Osiecki2021).

Studies of the river valley bottom sediments have confirmed the presence of slags of different ages, mostly where archaeological work did not reach, like at the Doły Biskupie site (Klatka, Reference Klatka1958), or in other rivers in the Holy Cross Mountains, like Czarna Nida (Przychodni, Reference Przychodni and Orzechowski2002, Reference Przychodni, Orzechowski and Suliga2006; Krupa, Reference Krupa2013, Reference Krupa2015). Further research in the Świślina River using new methods revealed changes in sediments, indicating new possibilities of interpreting the results obtained (Kalicki et al. Reference Kalicki, Przepióra, Frączek, Fularczyk, Żurek, Pabian, Podrzycki, Ratajczak-Skrzatek, Kovalchuk and Stefaniak2021a, Reference Kalicki, Przepióra, Fularczyk, Houbrechts, Cunha, Fontana and Panin2021b), and attempted to relate them to prehistoric or contemporary anthropogenic factors. These studies could be used as comparative material from other sites, where similar analyses in the OPID area have already been carried out (Przepióra et al. Reference Przepióra, Kalicki, Chwałek and Houbrechts2019, Reference Przepióra, Kalicki, Aksamit, Aksamit, Fularczyk, Kusztal, Houbrechts, Cunha, Fontana and Panin2021, 2022a, 2022b; Kalicki et al. Reference Kalicki, Przepióra, Chwałek, Aksamit, Grzeszczyk and Houbrechts2021c, Reference Kalicki, Przepióra, Kusztal, Fularczyk and Houbrechts2023) and will continue in the future.

STUDY AREA

The research area is located in the northeastern part of the Świętokrzyskie Voivodeship in the western part of the Kunów commune near the village of Doły Biskupie in the lower reach of the Świślina River (Fig. 1). The Świślina River, a 36-km-long right tributary of the Kamienna River, belongs to the middle Vistula River basin. Its sources are located at an altitude of 343.9 m near the village of Siekierno and the confluence at 177.3 m above sea level (m asl) (Bado, Reference Bado2012). The average slope of the river is approximately 4.6‰ (from its sources to the confluence of Pokrzywianka River is 6‰ and 1.5‰ in the lower course) (Śliwa, Reference Śliwa, Kloss and Kurzelewski2007). The riverbed is meandering. The sinuosity index is 1.51 for the entire river length and 1.56 downstream of the Wióry Reservoir. In its middle section, the riverbed is approximately 3.5–4.0 m wide and 6–7 m downstream of the Wióry Reservoir (Bado, Reference Bado2012). The Świślina River and its tributaries have a pluvial–nival regime characterized by high variability and a significant amplitude of extreme daily and seasonal flows. There are two peaks in the outflow: in March and April (caused by snow supply) and in May and June (caused by rain supply). There are three extreme flows in the lower (Nietulisko Duże village) section: February/March, July, and October (Kupczyk et al., Reference Kupczyk, Biernat, Ciupa, Kasprzyk and Suligowski1994; Koślacz et al., Reference Koślacz, Suligowski, Szymanek, Daszkiewicz, Jendo, Jendo and Kasprzyk2006; Suligowski et al., Reference Suligowski, Kupczyk, Kasprzyk and Koślacz2009; Bado, Reference Bado2012).

Figure 1. Location of the study area within a sketch map of the Europe (inset). The Świślina drainage basin (blue limit) and research area (red box) are shown on the Świętokrzyskie Voivodship Digital Elevation Model (DEM; created by M. Frączek on the basis of data obtained from CODGiK, MGGP Aero, no. GI-FOTO.703.44.2014) with physicogeographic mesoregions (1–3) of Poland in the catchment area (Kondracki, Reference Kondracki1977, Reference Kondracki2002): 1, Suchedniów Plateau (342.36); 2, Holy Cross Mountains (342.34-35); 3, Sandomierz Upland (342.36).

The Świślina's 414 km2 catchment area is located in the Kielce Upland and is extremely asymmetric, with almost no left-side tributaries. It covers fragments of three physicogeographic mesoregions: Suchedniów Plateau (the upper and middle course of the Świślina basin), the Holy Cross Mountains, and the Sandomierz Upland (Fig. 1) (Kondracki, Reference Kondracki1977, Reference Kondracki2002; Solon et al., Reference Solon, Borzyszkowski, Bidłasik, Richling, Badora, Balon and Brzezińska-Wójcik2018; Richling et al. Reference Richling, Solon, Macias, Balon, Borzyszkowski and Kistowski2021). The catchment is located in the eastern forelands of the Holy Cross Mountains, in the geomorphological macroregion of the Kielce Upland subprovince (Klimaszewski, Reference Klimaszewski1978). The Świślina River valley marks the border between two mesoregions: the Opatów (Sandomierz) Upland (to the SE), and the Suchedniów Plateau (to the NW).

The study area is located in the northeastern part of the Mesozoic margin of the Holy Cross Mountains, north of the Łysogóry main range (Wróblewski and Wróblewska, Reference Wróblewski and Wróblewska1996). In this monocline, there is a predominant NW-SE strike and a NE dip of the layers. Among the Mesozoic rocks, there are two basic lithological complexes: the lower one, dominated by clastic rocks (mainly sandstone, mudstone, conglomerates, and clays from the Lower Triassic to the Middle Jurassic) and the upper one, which consists of chemical–zoogenic rocks (various types of limestone, marl, and oolite from the Upper Jurassic to the Upper Cretaceous) (Kosmowska-Suffczyńska, Reference Kosmowska-Suffczyńska2000). The Świślina River valley near the village of Doły Biskupie is crossed transversely SE-NW by the Godów-Mnichów fold, containing the oldest rocks (from the Lower Triassic) in the whole basin (Filonowicz, Reference Filonowicz1966, Reference Filonowicz1968).

A characteristic feature of this relief area is the vast, monotonous surfaces of the Palaeogene peneplain, which cut both the fold structure of the Palaeozoic core and the large radial undulations of the Mesozoic bedrock. The basement in most of the catchment area is covered with Pleistocene loess. Locally in the valleys, there are also fluvioglacial sands and gravels of the South-Polish (San) glaciations and Vistulian sandy-gravel alluvia (Fig. 2). Their thickness ranges from 3 to 6 m and builds an erosive–accumulative terrace up to 1.5 m above the Holocene floodplain (Filonowicz, Reference Filonowicz1968; Bado, Reference Bado2012). The Holocene fine alluvium (mainly overbank facies) is made of redeposited loess (Klatka, Reference Klatka1958) and weathered Silurian clay slates and flood rhythmites near Nietulisko (Filonowicz, Reference Filonowicz1968). The Pleistocene loess is cut by a dense network of many young erosive forms—gullies, arroyos, and sunken lanes, which are also intensively modelled today. Headward erosion can withdraw the source funnel of such a form up to 20 m/yr (Klatka, Reference Klatka1958).

Figure 2. Geological structure of the Świślina catchment near the study site (red box) based on Detailed Geological Map of Poland 1:50,000, sheet Słupia Nowa(Filonowicz, Reference Filonowicz1966; www.pgi.gov.pl).

AIM OF THE STUDY AND METHODS

The study aims to identify the structure, especially the anthropogenic factor, of the Świślina River valley bottom in the Doły Biskupie village vicinity and to confirm and refine the results of valley sediment studies from the 1950s (Klatka, Reference Klatka1958) with an emphasis on prehistoric and medieval metallurgical activity impact using new research methods. Results were compared with archaeological data to verify the impact of the anthropogenic factor and the period when it occurred. This is pioneering research in the Holy Cross Mountains, based on microscopic residue from the iron smelting found in the analysis of the alluvia. The results may be used to reinterpret the accumulation processes of other river valleys in the OPID area (Fig. 3).

During field research, the DB1 profile was made on the left accumulative bank, and samples were taken for laboratory analysis. This profile represents the structure of the floodplain. About 40 m NW from the DB1 on the terrace, two other profiles (K1 and 2) were made earlier by Klatka (Reference Klatka1958). Presently, the edge is completely overgrown with bushes and covered with turf, making it impossible to uncover these profiles again. For this reason, the archival profiles described in the 1950s were used in this paper.

Seven samples were taken from the profile and dried to prepare them for analysis. The grain-size analysis was carried out using a set of sieves measuring from 2800 to 63 μm (DIN ISO 3310/1) and the Retsch-Rahmen at the Geomorphological and Hydrological Laboratory of the Department of Geomorphology and Geoarchaeology at the Institute of Geography and Environmental Sciences at the Jan Kochanowski University in Kielce (Poland). All sandy samples were identical in weight (100 g) to obtain meaningful and comparable results. The finer deposit (<1 mm) measurements were made in the Mastersizer 3000 particle size analyser (Malvern Instruments Ltd). The GRANULOM program was used to graphically process the results. This program enables the calculation of Folk and Ward (Reference Folk and Ward1957) grain size–distribution parameters.

Geochemical analyses included pH determination using the potentiometric method with the ELMETRON CP-411 pH meter, made by suspension of samples in distilled water in a 1:2.5 ratio. The CaCO3 content was determined using Scheibler's method. The selected heavy metal element contents in the sediments were analysed with the help of Jan Horák (University of Hradec Králové). An XRF-type BAS Delta HHXRF analyser spectrometer from the Delta Professional series was used. The X-ray fluorescence spectrometry (XRF) method is based on measuring the fluorescent radiation that begins to be emitted from the sample when it is bombarded with high-energy X-rays. This method enables the identification of elements and determines their concentration. The spectrometer automatically measured each sample three to five times, and the results were averaged. The concentrations of five elements were measured (Cu, Zn, Pb, Mn, and Fe), and the values are presented in milligrams per kilogram. For the device used in this study, the following limits of quantification were determined for each of the elements: Cu = 5–7 mg/kg, Zn = 3–5 mg/kg, Pb = 2–4 mg/kg, Mn = 10 mg/kg, and Fe = 10 mg/kg (0.001%) (Kłusakiewicz, Reference Kłusakiewicz2019).

The magnetic spherule separation (MSS) method was also applied. This method has so far been used mainly by researchers in the Ardennes area (Belgium) (Richardeau, Reference Richardeau1977; Houbrechts et al., Reference Houbrechts, Petit, Notebaert, Kalicki and Denis2020). The MSS method, slightly modified, consists of sifting the dry sample through a set of sieves to obtain a material with a 200–63 μm size range. Depending on the ferromagnetic particle, from 1 to 10 g of material was used, which facilitates further conversion of the concentration of iron spherules in the sediments (in special cases, the weight may change). The material from the compartment obtained is spread on a tray or a piece of white paper. The sample is spread over the surface by sliding a precision magnetic gripple to separate the ferromagnetic particles from the rest of the sediment. These particles are transferred from the gripple to a microscope slide with a piece of self-adhesive double-sided tape. The material is carefully spread over the tape to keep it firmly attached. The characteristic microscopic iron balls (number of magnetic spherules per gram of material, ms/g) are counted manually under the microscope. Data were standardized and presented as magnetic spherules per 10 g in order to highlight the results obtained.

The cameral research consisted of an historical and archaeological materials query, including previous publications about the study area. Graphical processing of the laboratory results obtained was also done with CorelDraw.

RESULTS

A river gap section with steep valley slopes near Doły Biskupie, cut in the soft Lower Triassic and the Pliocene–Pleistocene rocks, separates two flat plateaus. There are remnants of the Palaeogene planation surface cutting the monoclonal Triassic inclines, which descend with steep edges 50–60 m high into the Świślina River valley. The edges of the main valley are cut by many smaller dry erosion valleys created in different ages. In the right valley slope, there is a clear levelling (plain), which could be interpreted as a rock or erosive–accumulative terrace, but the thick layer of loess masks the deeper geologic structure and the original morphology. The study site is located in this section at the estuary of the former paper mill canal (Fig. 4). Two levels can be distinguished in the valley bottom: a terrace (11–9 m arl) represented by the K1 and K2 profiles (Klatka, Reference Klatka1958; Fig. 5) and a floodplain (5.5–4.5 m arl) represented by the DB1 profile (Fig. 6).

Figure 3. The Old-Polish Industrial District (OPID) border based on M. Radwan's map (Bielenin, Reference Bielenin1992), with updated bloomery activity areas based on A. Przychodni (Reference Przychodni and Orzechowski2002). Study site location is in the Świślina catchment area (adapted by P. Przepióra).

Figure 4. Study area on the Digital Elevation Model (DEM) showing profile locations (red arrows), borders of the terrace and floodplain levels (red dotted line), and loess upland (orange dotted line) (www.geoportal.gov.pl).

Figure 5. The K1 and K2 profiles of the Świślina terrace at Doły Biskupie (Klatka, Reference Klatka1958; adapted by Ł. Podrzycki and P. Przepióra).

Figure 6. View of the study site towards the river (left) and the location of the DB1 profile (photo by T. Kalicki 2014).

K1 and K2 profiles (Klatka Reference Klatka1958)

Both outcrops were recorded and analysed by Klatka (Reference Klatka1958) on the edge of the terrace. In its upper part, it is built up by overbank sediments consisting of silt and sandy silt. A large fragment of slag and iron was found in the silt intercalation of fine sand at a depth of 5 m. Charcoal occurs above 3.5 m and below 6.5 m (K1). At K2, slag and charcoal were deposited more shallowly at a depth of 2.5–1.0 m (Fig. 5). Slag and charcoal are traces of the prehistoric and medieval metallurgy (Klatka, Reference Klatka1958). There are channel sediments in the lower part of each profile. These are indicated by their structure and texture—medium- and fine-grained sand, bedded with the subfossil trunks.

Profile DB1

There is channel sediment in the lower part—sand with gravel (mean size [Mz] approx. 1.2ø), moderately well sorted (approx. standard deviation [σI] = 0.7), containing carbonate (approx. 14% CaCO3 content). It is covered by overbank sediment more than 2 m thick that is composed of silt-sandy sediment (with a portion of fine sand up to 25–40%; Mz = 4–5ø) with a poorly expressed fining upward tendency, poorly sorted (σI from 1.1 to 1.7). In the alluvium there are two distinct sandy intercalations at depths of 1.6 m and approximately 1.0 m. The CaCO3 content drops upward from approximately 14 to 2%, which causes the pH to change from neutral to slightly acidic. Geochemical analysis of selected elements (Cu, Zn, Pb, Mn, Fe) also shows an increase in their content upward of the profile, especially Cu and Pb. This tendency is visible throughout the profile but becomes clearest above the sandy layer from a depth of approximately 1.6 m (Fig. 7).

Figure 7. DB1 grain-size profile with Folk and Ward (Reference Folk and Ward1957) grain size–distribution parameters; CaCO3 content; sediment pH; concentrations of selected elements (Cu, Zn, Pb, Mn, Fe); and the microslag content in magnetic spherules per 10 g of matter (ms/10 g) with the probable level where sediment accumulation began after the period of metallurgical activity (red, dashed line).

Macroscopic traces of the occurrence of larger slag fragments on the macro- (centimetres) and microscale (millimetres) were not detected anywhere in the profile. However, the separation of magnetic spherules (microslags) showed their occurrence. They were detected above the sandy layer at a depth of 1.6 m, from about 10 to 25 pieces/10 g of sediment. Their maximum is at depth of 1.0–0.3 m (in and above the second sandy layer). This maximum coincides with the abrupt increase in all five measured metals in the profile content: Fe (from approx. 3000 to 120,000 mg/kg), Mn (from approx. 100 to 300 mg/kg), Zn (from approx. 5 to 50 mg/kg), Cu (from 0 to 22 mg/kg), and Pb (from 3 to 20 mg/kg) (Fig. 7).

DISCUSSION

Klatka (Reference Klatka1958) discovered charcoal and slag in sediment connected with the prehistoric and medieval metallurgical activity in this region on the left bank of Świślina River in the 1950s. The Świślina River basin is located in the eastern part of the OPID, where ancient metallurgy dominated (Fig. 3). Slag from the prehistoric bloomeries was detected in almost the entire Świślina catchment area (Radwan, Reference Radwan1963; Bielenin, Reference Bielenin1992). Metallurgy was most likely still active here in the Middle Ages, but there is no information about forges along the river on archival maps, even from the modern period. Also, examining historical materials did not reveal the presence of metallurgical furnaces in the vicinity (Zieliński, Reference Zieliński1965; Bielenin, Reference Bielenin1992). The ruins of a modern rolling mill (a sheet metal works) at Nietulisko Duże near the estuary connecting the Świślina to the Kamienna River (Suliga, Reference Suliga1995), dating from the nineteenth century, are the only remnants of modern metallurgical activity close to the study site. Also, a former paper mill 400 m upstream from the study site was previously in operation until the 1980s.

The traces of the metallurgical industry are mainly macroscopic slag fragments and iron spherules (Dungworth and Wilkes, Reference Dungworth and Wilkes2007). Their absence in the sediment, however, does not mean that there was no metallurgical activity in the immediate vicinity. Slag can be redeposited during high river discharges or floods. The last large flood took place when the embankment built during the construction of the Wióry Reservoir in 2001 was destroyed after heavy rain (Biernat and Ciupa, Reference Biernat, Ciupa, Ludwikowska-Kędzia and Wiatrak2007; Ciupa, Reference Ciupa, Szwarczewski and Smolska2012). Very similar catastrophic events on rivers in the Holy Cross Mountains have occurred quite often in the past. Historical materials show, for example, in the Czarna Konecka and Kamionka Rivers (Kalicki et al., Reference Kalicki, Przepióra and Kusztal2019a, Reference Kalicki, Przepióra and Kusztal2019b; Przepióra, Reference Przepióra and Kalicki2021), many flash flood events taking place in the twentieth century or even the nineteenth century after anthropogenic small-scale water-retention system hydrotechnical structure failure (Kalicki et al., Reference Kalicki, Frączek, Przepióra, Kusztal, Kłusakiewicz and Malęga2019c, Reference Kalicki, Przepióra, Kusztal, Chrabąszcz, Fularczyk, Kłusakiewicz and Frączek2020). The presence of magnetic iron spherules in sediments should also be interpreted in terms of their redeposition during catastrophic floods from this period. Usually, this material is transported by the wind (aeolian transport) up to 10 km from the source (e.g., bloomeries) and only later redeposited by fluvial processes (Houbrechts et al. Reference Houbrechts, Petit, Notebaert, Kalicki and Denis2020). The occurrence of macro- and microslags in the sediments of the Świślina floodplain can therefore be interpreted as traces of prehistoric (Roman period) and probably medieval metallurgy in the catchment area of the OPID (Radwan, Reference Radwan1963; Bielenin, Reference Bielenin1992; Orzechowski, Reference Orzechowski2007).

The Świślina floodplain in the study area is composed mainly of sandy silts (Figs. 6 and 7). There is a distinct sand and gravel layer on the bottom (lag deposits), and at a depth of 1.6 m there is a thin layer of sandy overbank sediment. The CaCO3 content increases with depth and reaches its highest value (about 14%) at the depth of the lag deposits. It is most likely related to the geologic structure, where the lag level consists of (among others) limestone, but the CaCO3 content may also be influenced by the remains of malacofauna. There is also a visible pH increase in the profile ranging from slightly acidic to neutral, and even alkaline.

Geochemical analysis also showed a clear increase in the content of selected heavy metal elements in the sediments where iron spherules were detected (Fig. 7). The increase in the Fe, Mn, Zn, Cu, and Pb content perfectly reflects the appearance of metallurgical residues in floodplain sediments at the same depths. A similar situation was described in the Kamionka River valley, where a significant increase in Fe content was noted in sediment with metallurgical slag (Przepióra, Reference Przepióra and Kalicki2021). Near the study area there is a lack of major roads, rail tracks, or industrial facilities as potential sources of trace metals. Agricultural processes, however, could provide an alternate explanation for such pollutants in the soil.

The report from the years 1995–2015 (Kiczor, Reference Kiczor and Tkaczuk2017) shows the geochemical background (samples from the Doły Biskipie site were collected and analysed in 2014). The nearest soil measurement stations in terms of contamination with selected trace elements are in Wąchock (approx. 20 km NW) and Ćmielów (approx. 24 km E). Acidic soils with a pH from 4.6 to 5.0 predominate in the study area. None of the trace elements in the study area exceeded the norms during the study period. Only in Ćmielów was a higher Pb content detected, at approximately 70 mg/kg in 2015. However, the soil was still classified as slightly contaminated. The concentration of Cu was only 8 mg/kg, and Zn about 35 mg/kg. The values at the measurement point in Wąchock were very similar. Only Cu exceeded 30 mg/kg during the measurement period, and this value dropped to 3 mg/kg in 2015. The soils in the study area have a natural content of specific chemical components. The lack of major changes in the concentration of the measured substances or elements indicates a slight anthropogenic impact (Kiczor, Reference Kiczor and Tkaczuk2017). These data confirm that the geochemical results from Doły Biskupie are within the limits of trace material contents shown in the report.

Many iron spherules were detected in the sediment above the flood layer at 1.6 m. These are most likely traces of the prehistoric (Roman period) or medieval metallurgical activity that Klatka (Reference Klatka1958) wrote about. It has been experimentally confirmed that microscopic artefacts are of anthropogenic origin and can act as tracers for metallurgical activity (Dungworth and Wilkes, Reference Dungworth and Wilkes2007). Iron spherules occur only above the flood layer, which may suggest that the younger sediments of the floodplain were deposited by the river during the period of metallurgical activity in the Świślina basin. However, there are no data about larger metallurgical plants from the last few centuries operating on the Świślina River, apart from the nineteenth-century sheet metal works in the confluence at Nietulisko Duże, downstream of the study site. The detection of microspherules in alluvia redeposited by the river excludes the possibility that they are product of activity of later forges in the nearby Kamienna valley. However, there is only one known historical iron factory in the central part of Świślina catchment (Fig. 3). A single instance of metallurgical activity at a great distance would not contribute microspherules to the Doły Biskupie study site.

Of greater importance are traces of the largest concentration of prehistoric metallurgical activity in this part of Europe that have been preserved in this area (e.g., Orzechowski, Reference Orzechowski2007). Microspherules were most likely redeposited by the river from Świślina catchment area, especially the upper section of the river, where prehistoric metallurgy was more intense. There is a much larger number of bloomery sites, the density of which is estimated to be up to 50–100 for 1 km2. In the immediate vicinity of Doły Biskupie, there are far fewer of these sites, but the estimated density based on the inventory is up to 30 for 1 km2 (Fig. 8). As Klatka (Reference Klatka1958) suggested, large fragments of slag detected in the K1 and K2 profiles, due to their size and location, could rather be of local smelting origin (in situ). Because they are in fluvial cut and fill, however, this slag was most likely also redeposited from a site at a much shorter distance. Unfortunately, it is impossible to accurately determine the age of slag found in the sediments based only on the Klatka (Reference Klatka1958) work.

Figure 8. The main area of ancient iron metallurgy in the Holy Cross Mountains based on the 1950–1990 inventory results of K. Bielenin, Sz. Orzechowski, and T. Wichman (adapted by Rubinowski [1992], and later by P. Przepióra).

The study site in Doły Biskupie is located in the gap section of the river and lack of historical metallurgy activity in its basin confirms that iron spherules found here may be an indicator of the prehistoric metallurgical activity from the entire Świślina catchment area (Fig. 8). Relatively few iron spherules were present in the Świślina River alluvia (less than 30 in 10 g of material) compared with other research results, for example, from the Ardennes rivers (Belgium) (more than 100 in 1 g of material) (Houbrechts et al., Reference Houbrechts, Petit, Notebaert, Kalicki and Denis2020) or from the Kamionka River (Poland) (more than 25 in 1 g of material) (Przepióra et al., Reference Przepióra, Kalicki, Houbrechts and Kalicki2022a, 2022b), representing medieval and modern metallurgical activity study sites located near remnants of historical forges.

It should therefore be considered that the microscopic iron spherules preserved in the floodplain sediment are not in situ. This is confirmed by their location in the middle and upper part of the profile, above the clear flood sandy layer, which may signal fluvial events and changes in the Świślina basin. The redeposition process of microscopic artefacts in Świślina could be similar to those at the Czarna Konecka River (Przepióra et al., Reference Przepióra, Kalicki, Aksamit, Aksamit, Fularczyk, Kusztal, Houbrechts, Cunha, Fontana and Panin2021), where only a few spherules were found in young delta sediments (i.e., washing out the spherules from alluvia and river incision in older sediments without microartefacts). A large water reservoir built upstream from the study site at the beginning of the twenty-first century may currently restrict the delivery of the material, so iron spherules found in profile may have been deposited later during the catastrophic floods, for example, rupture of a dam in 2001 (cf. Biernat and Ciupa, Reference Biernat, Ciupa, Ludwikowska-Kędzia and Wiatrak2007; Ciupa, Reference Ciupa, Szwarczewski and Smolska2012).

Very comparable results were obtained in studies from river valleys of a similar mining and metallurgical district in Wallonia (Belgium), where the method of searching for macro- and microscopic slag as well as for magnetic iron spherules was applied (Houbrechts, Reference Houbrechts2007; Houbrechts et al., Reference Houbrechts, Petit and Kalicki2003, Reference Houbrechts and Petit2004, 2020; Houbrechts and Petit, Reference Houbrechts and Petit2003, Reference Houbrechts and Petit2004, Reference Houbrechts and Petit2006). However, these results concerned only medieval and post-medieval metallurgical activities, as confirmed by historical materials. This research was mostly done near a former forge. The MSS method has also recently been successfully used on other rivers of the Holy Cross Mountains, including the Kamionka River (Kalicki and Przepióra, Reference Kalicki, Przepióra, Chwałek and Frączek2019; Przepióra et al., Reference Przepióra, Kalicki, Chwałek and Houbrechts2019, Reference Przepióra, Kalicki, Houbrechts and Kalicki2022a, Reference Przepióra, Kalicki and Houbrechts2022b; Kalicki et al., Reference Kalicki, Przepióra, Chwałek, Aksamit, Grzeszczyk and Houbrechts2021c), where the medieval and modern metallurgical activity also predominated. A distinct postindustrial layer was also found, consisting of an accumulation of iron spherules within the floodplain, but this time from modern forges.

CONCLUSIONS

The Świślina River valley is a diverse area in terms of geology and relief due to the thicker loess deposits, which occur especially in its lower section. Many dry valleys and gullies indicate intense erosive processes. Transport of material by fluvial processes filled the valley bottom with silty and sandy sediments. Detailed analysis of sediment lying at the Świślina Valley bottom near Doły Biskupie show it is younger alluvium of the floodplain, with many macro- and microscopic artefacts related to the smelting of iron ore.

In the mid- twentieth century, traces of the prehistoric (Roman period) and medieval metallurgy (slags) were discovered in the terrace sediments. Modern research methods confirm the presence of a sediment layer that most probably accumulated during the period of bloomery activity, which was widespread in the Świślina basin in the OPID. Historical and cartographic materials, on the other hand, exclude the possibility that the slags were from the medieval or modern metallurgy period. They were deposited directly in the vicinity of the former metallurgical furnace or redeposited from the upper sections of the basin (e.g., during a flood), where the remains of bloomeries in the Holy Cross Mountains were discovered in great numbers.

The cause of geochemical changes in the study profile may be caused by natural (geologic structure) and anthropogenic factors (road transport and agriculture); however, iron spherules detected in the alluvium indicate the most likely source of these pollutants. The presence of microscopic artefacts in sediment with an increased content of trace elements may have been caused by an anthropogenic factor related to the prehistoric metallurgical activity. The Wióry Reservoir dam, built at the beginning of the twenty-first century, can effectively capture pollutants from the upper part of the catchment area. The iron spherules could have been redeposited from the upper catchment from before the dam construction during the flood of 2001, or they may also indicate the close presence of an additional bloomery site. Results obtained from the Świslina River valley, including the analysis of archaeological and historical data, might indicate that iron spherules from the prehistoric metallurgical activity (bloomery) period were detected for the first time using the MSS method.

MSS, combined with other methods, could be extremely useful in further research of other OPID catchments to study the human–environment relationship and could also contribute to detection of further bloomery sites in other river catchments of the Holy Cross Mountains region.

Acknowledgments

Special thanks to Jan Horák and Edyta Kłusakiewicz for help with field and laboratory work and to Brian Ground for translation and linguistic corrections of the paper.

References

REFERENCES

Alexandrowicz, S.W., 1996. Malacofauna of Late Holocene overbank deposits in southern Poland. Bulletin of the Polish Academy of Sciences, Earth Sciences 44, 235–249.Google Scholar
Bado, J., 2012. Antropogeniczne przekształcenia równiny zalewowej Świśliny poniżej Rzepina Kolonii. MSc thesis, Jan Kochanowski University, Kielce.Google Scholar
Bielenin, K., 1992. Starożytne górnictwo i hutnictwo żelaza w Górach Świętokrzyskich. Kieleckie Towarzystwo Naukowe, Kielce.Google Scholar
Biernat, T., Ciupa, T., 2007. Powódź w zlewni Świśliny w lipcu 2001 r. oraz jej skutki w strefie budowy zbiornika wodnego „Wióry” (Góry Świętokrzyskie). In: Ludwikowska-Kędzia, M., Wiatrak, M. (Eds.), Nauki Geograficzne w Badaniach Regionalnych Tom VIII: Różnorodność środowiska geograficznego Gór Świętokrzyskich w badaniach regionalnych. IG AŚ, Kielce, pp. 57–64.Google Scholar
Brown, A.G., Keough, M., 1992a. Holocene floodplain metamorphosis in the Midlands, United Kingdom. Geomorphology 4, 433–445.CrossRefGoogle Scholar
Brown, A.G., Keough, M., 1992b. Palaeochannels and palaeolandsurfaces: the geoarchaeological potential of some Midland floodplains. In: Needham, S., Macklin, M.G. (Eds.), Alluvial Archaeology in Britain. Oxbow Monograph 27. Oxbow Books, Barnsley, UK, pp. 185–196.Google Scholar
Ciupa, T., 2012. Przyrodnicze i antropogeniczne uwarunkowania oraz skutki powodzi w zlewni rzeki Świśliny w lipcu 2001 roku (Góry Świętokrzyskie). In: Szwarczewski, P., Smolska, E. (Eds.), Zapis działalności człowieka w środowisku przyrodniczym. Wydawnictwa Uniwersytetu Warszawskiego, Warszawa, pp. 29–34.Google Scholar
Dungworth, D., Wilkes, R., 2007. An Investigation of Hammerscale: Technology Report. Research Department Report 26. English Heritage, Portsmouth, UK.Google Scholar
Filonowicz, P., 1966. Szczegółowa Mapa Geologiczna Polski w skali 1:50 000. Arkusz Nowa Słupia Wydawnictwo Geologiczne, Warszawa.Google Scholar
Filonowicz, P., 1968. Objaśnienia do szczegółowej mapy geologicznej Polski w skali 1:50 000. Arkusz Nowa Słupia Wydawnictwo Geologiczne Warszawa.Google Scholar
Folk, R.L., Ward, W.C., 1957. Brazos River bar: a study in the significance of grain size parameters. Journal of Sedimentary Petrology 27, 3–26.CrossRefGoogle Scholar
Hempel, L., 1956. Über Alter und Herkunftsgebiet von Auelehmen im Leinetal. Eiszeitalter und Gegenwart 7, 35–42.Google Scholar
Hempel, L., 1976. Bodenerosion und Auelehm. In: Richter, G. (Ed.), Bodenerosion in Mitteleuropa [reprint from 1959]. Wege der Forschung 430. Wissenschaftliche Buchgesellschaft, Darmstadt, pp. 331–333.Google Scholar
Hiller, A., Litt, T., Eissmann, L., 1991. Zur Entwicklung der jungquartären Tieflandstäler im Saale-Elbe-Raum unter besonderer Berücksichtigung von l4C-Daten. Eiszietalter und Gegenwart 41, 26–46.Google Scholar
Hong, S.J., 1995. Holozäne und aktuelle Tal- und Flussetwicklung auf der Nordostabchandung des Kaufunger Waldes, Nordhessen. Dissertation der Georg-August Universität zu Göttingen.Google Scholar
Houben, P., 2003. Spatio-temporally variable response of fluvial systems to Late Pleistocene climate change: a case study from central Germany. Quaternary Science Reviews 22, 2125–2140.CrossRefGoogle Scholar
Houbrechts, G., 2007. La sidérurgie proto-industrielle dans le bassin de la Lienne, de la Meuse à l'Ardenne. Entre Ardenne et Meuse ASBL 39, 34–63.Google Scholar
Houbrechts, G., Petit, F., 2003. Utilisation des scories métallurgiques en dynamique fluviale: détermination de la compétence effective des rivières et estimation des vitesses de progression de leur charge de fond/Utilisation of metallurgie slags for the study of fluvial dynamics: determination of the effective competency of rivers and estimation of the transit time of sedimentary waves. Géomorphologie: Relief, Processus, Environnement, Janviermars 9, no. 1, 3–12.CrossRefGoogle Scholar
Houbrechts, G., Petit, F., 2004. Evolution des techniques sidérurgiques préindustrielles et aperçu des critères de localisation de la métallurgie en «Terre de Durbuy». Terre de Durbuy 89, 3–29.Google Scholar
Houbrechts, G., Petit, F., 2006. Utilisation des microscories métallurgiques comme traceur de la sédimentation dans les plaines alluviales des rivières ardennaises. University of Liege, Liege, pp. 95–98.Google Scholar
Houbrechts, G., Petit, F., Kalicki, T., 2003. Metallurgic slags of the last centuries as a tracer in archaeological and palaeogeographical studies in Arden (Belgium). In: Final Programme and Abstracts of 9th Annual Meeting of European Association of Archaeologists, 10th–14th September 2003, St. Petersburg, pp. 17–18.Google Scholar
Houbrechts, G., Petit, F., Kalicki, T., 2004. Rozwój metalurgii a sedymentacja fluwialna z ostatnich stuleci w ardeńskich dopływach Mozy (Belgia). In: Michalczyk, Z. (Ed.), Badania geograficzne w poznawaniu środowiska. Maria Curie-Skłodowska University Press, Lublin, pp. 192–194.Google Scholar
Houbrechts, G., Petit, F., Notebaert, B., Kalicki, T., Denis, A.C., 2020. Microslag as a stratigraphic tracer to quantify floodplain processes (Lienne catchment, Belgium). Geomorphology 360, 107166.CrossRefGoogle Scholar
Huckriede, R., 1971. Über jungholozäne, vorgeschichtliche Löß-Umlagerung in Hessen. Eiszeitalter und Gegenwart 22, 5–16.Google Scholar
Janiec, J., Kardyś, P., 2021. Baza surowcowa starożytnego hutnictwa regionu świętokrzyskiego – Próby innego spojrzenia. In: Dąbrowski, A., Osiecki, J. (Eds.), Świętokrzyskie. Środowisko, dziedzictwo kulturowe i edukacja regionalna, Vol. 27, no. 31. Wojewódzka Biblioteka Publiczna im. Witolda Gąbrowicza w Kielcach, pp. 173–182.Google Scholar
Jäger, K.D., 1962. Ober Alter und Ursachen der Auelehmablagerung thüringischer Flüsse. Praehist Z 40, 1–59.CrossRefGoogle Scholar
Kalicki, T., 2006. Zapis zmian klimatu oraz działalności człowieka i ich rola w holoceńskiej ewolucji dolin środkowoeuropejskich. Prace Geograficzne 204. Instytut Geografii i Przestrzennego Zagospodarowania PAN, Warszawa.Google Scholar
Kalicki, T., Przepióra, P. (coop. with Chwałek, S., Frączek, M.), 2019. Lokalizacja oraz zasięg historycznego układu hydrotechnicznego z młynem wodnym w Jędrowie (obecnie: ul. Koszykowa 18b w Suchedniowie). Geoarchaeological expertise commissioned by the Voivodeship Conservator of Monuments in Kielce.Google Scholar
Kalicki, T., Przepióra, P., Kusztal, P., 2019a. Antropogeniczne powodzie błyskawiczne na dwóch wybranych rzekach Świętokrzyskich w XX w. - Przyczyny i skutki. Prace i Studia Geograficzne, Warszawa 64, no. 1, 21–36.Google Scholar
Kalicki, T., Przepióra, P., Kusztal, P., 2019b. Origin and effects of anthropogenic flash floods on rivers of Holy Cross Mts. region (Poland) in 20th c. Acta Geobalcanica 5, no. 2, 85–92.CrossRefGoogle Scholar
Kalicki, T., Frączek, M., Przepióra, P., Kusztal, P., Kłusakiewicz, E., Malęga, E., 2019c. Late Quaternary geomorphology and geoarchaeology in the rivers of the Holy Cross Mountains region, Central Europe. Quaternary Research 91, 584–599.CrossRefGoogle Scholar
Kalicki, T., Przepióra, P., Frączek, M., Fularczyk, K., Żurek, K., Pabian, G., Podrzycki, Ł., 2021a. Natural and anthropogenic environment changes in Świślina valley—case study from Doły Biskupie site (Poland). In: Ratajczak-Skrzatek, U., Kovalchuk, O., Stefaniak, K. (Eds.), Proceedings of INQUA SEQS 2021 Conference, Quaternary Stratigraphy—Palaeoenvironment and Humans in Eurasia. University of Wrocław and Polish Geological Society, Wrocław, pp. 44–45.Google Scholar
Kalicki, T., Przepióra, P., Fularczyk, K., Houbrechts, G., 2021b. Macro- and microscopic slags as a marker of the metallurgical activity in the Holy Cross Mountains, Poland. In: Cunha, P., Fontana, A., Panin, A. (Eds.), FLAG 2021 Abstract Book. Institute of Geography Russian Academy of Sciences, Moscow, pp. 39–42.Google Scholar
Kalicki, T., Przepióra, P., Chwałek, S., Aksamit, M., Grzeszczyk, P., Houbrechts, G., 2021c. The Jędrów historic hydrotechnical system—a geoarchaeological and restoration studies (Holy Cross Mountains, Poland). Acta Geobalcanica 7, 123–129.CrossRefGoogle Scholar
Kalicki, T., Przepióra, P., Kusztal, P., Chrabąszcz, M., Fularczyk, K., Kłusakiewicz, E., Frączek, M., 2020. Historical and present-day human impact on fluvial systems in the Old-Polish Industrial District (Poland). Geomorphology 367, 107062.CrossRefGoogle Scholar
Kalicki, T., Przepióra, P., Kusztal, P., Fularczyk, K., Houbrechts, G., 2023. Microscale iron spherules as a trace of metallurgical activity in Old-Polish Industrial District river valleys. Miscellanea Geographica 27, 1–7.CrossRefGoogle Scholar
Kiczor, B., 2017. Gleby. In: Tkaczuk, U. (Ed.), Stan środowiska w województwie świętokrzyskim. Raport 2017. Wojewódzki Inspektorat Ochrony Środowiska, Kielce, pp. 135–146.Google Scholar
Klatka, T., 1958. Muły antropogeniczne doliny Świśliny i ich dynamiczna interpretacja. Łódzkie Towarzystwo Naukowe, Wydz. III 54, 165–187.Google Scholar
Klimaszewski, M., 1948. Polskie Karpaty Zachodnie w okresie dyluwialnym. Prace Wrocławskiego. Towarzystwa Naukowego, series B, 7.Google Scholar
Klimaszewski, M., 1978. Geomorfologia. PWN, Warszawa.Google Scholar
Klimek, K., 1988. An early anthropogenic alluvialion in the Subcarpathian Oświęcim Basin, Poland. Bulletin of the Polish Academy of Sciences, Earth Sciences 36, 159–169.Google Scholar
Klimek, K., 1996. Aluwia Rudy jako wskaźnik 1000-letniej degradacji Płaskowyżu Rybnickiego. In: Kostrzewski, A. (Ed.), Geneza, litologia i stratygrafia utworów czwartorzędowych, tom II. UAM, Poznań, pp. 155–166.Google Scholar
Klimek, K., 2003. Sediment transfer and storage linked to Neolithic and Early Medieval soil erosion in the Upper Odra Basin, southern Poland. In: Howard, A.J., Macklin, M.G., Passmore, D.G. (Eds.), Alluvial Archaeology in Europe. Balkema, Rotterdam, pp. 251–259.Google Scholar
Klimek, K., Malik, I., Owczarek, P., Zygmunt, E., 2003. Climatic and human impact on episodic alluviation in small mountain valleys, the Sudetes. Geographia Polonica 76, 55–64.Google Scholar
Kłusakiewicz, E., 2019. Zróżnicowanie facjalne i geochemiczne aluwiów równiny zalewowej górnej Kamiennej (Wyżyna Kielecka). PhD thesis, Jan Kochanowski University, Kielce.Google Scholar
Kondracki, J., 1977. Regiony fizycznogeograficzne Polski. Wydawnictwo Uniwersytetu Warszawskiego, Warszawa.Google Scholar
Kondracki, J., 2002. Geografia regionalna Polski. PWN, Warszawa.Google Scholar
Kosmowska-Suffczyńska, D., 2000. Wpływ drobnych struktur tektoniki dysjunktywnej na kierunkowość rzeźby w północno-wschodnim obrzeżeniu Gór Świętokrzyskich, Geologia i geomorfologia Gór Świętokrzyskich—kontrowersje i nowe spojrzenia. Prace Instytutu Geografii Wyższej Szkoły Pedagogicznej, Kielce, pp. 171–208.Google Scholar
Koślacz, R., Suligowski, R., Szymanek, B., Daszkiewicz, J., Jendo, J., Jendo, A., Kasprzyk, A., et al., 2006. Program małej retencji dla województwa świętokrzyskiego. Świętokrzyski Zarząd Melioracji i Urządzeń Wodnych w Kielcach, Wrocław.Google Scholar
Krupa, J., 2013. Naturalne i antropologiczne procesy kształtujące dno doliny Czarnej Nidy w późnym vistulianie i holocenie. Folia Quaternaria 81, 5–156.Google Scholar
Krupa, J., 2015. Natural and anthropogenic channel pattern changes in the mid-mountain valley during the Late Glacial and Holocene, Polish Uplands. Quaternary International 370, 55–65.CrossRefGoogle Scholar
Kukulak, J., 2004. Zapis skutków osadnictwa i gospodarki rolnej w osadach rzeki górskiej na przykładzie aluwiów dorzecza górnego Sanu w Bieszczadach Wysokich. Wydawnictwo Naukowe Akademii Pedagogicznej, Kraków.Google Scholar
Kupczyk, E., Biernat, T., Ciupa, T, Kasprzyk, A., Suligowski, R., 1994. Zasoby wodne dorzecza Nidy. Wyższa Szkoła Pedagogiczna, Kielce.Google Scholar
Linke, W., 1976. Frühestes Bauerntum und geographische Umwelt. Bochumer Geographische Arbeiten 28, 86.Google Scholar
Lipps, S., 1988. Fluviatile Dynamik im Mittelwesertal während des Spätglazials und Holozäns. Eiszeitalter und Gegenwart 38, 78–86.Google Scholar
Litt, T., 1992. Investigations on the extent of the Early Neolithic settlement in the Elbe-Saale region and on its influence on the natural environment. In: Frenzel, B. (Ed.), Evaluation of Land Surfaces Cleared from Forests by Prehistoric Man in Early Neolithic Times and the Time of migrating Germanic Tribes. Special Issue: ESF Project European Palaeoclimate and Man 3. Paläoklimaforschung 8, 83–91.Google Scholar
Loźek, V., 1976. Zur Geschichte der Bodenerosion in den mitteleuropäischen Lössland schaften während des Holozäns. Newsletters on Stratigraphy 5, 44–54.Google Scholar
Lüttig, G., 1960. Zur Gliederung des Auelehms im Flußgebiet der Weser. Eiszeitalter und Gegenwart 11, 39–50.Google Scholar
Mäckel, R., 1969. Untersuchungen zur jungquartären Flussgeschichte der Lahn in der Giessener Talweitung. Eiszeitalter und Gegenwart 20, 138–174.Google Scholar
Mäckel, R., Zollinger, G., 1995. Holocene river and slope dynamics in the Black Forest and Upper Rhine Lowlands under the impact of man. In: Hagedorn, J. (Ed.), Late Quaternary and Present-Day Fluvial Processes in Central Europe. Zeitschrift für Geomorpholgie, Supplementband 100, 89–100.Google Scholar
Mensching, H., 1951a. Akkumulation und erosion niedersächsischer Flüsse seit der Risseiszeit. Erdkunde 5, 60–70.CrossRefGoogle Scholar
Mensching, H., 1951b. Die kulturgeographische Bedeutung der Auelehmbildung. In: Deutsche Geographentag Frankfurt/Main, Tagungsber und wiss Abhandlungen. Verlag des Amtes für Landeskunde, Remagen, Germany, pp. 219–225.Google Scholar
Mensching, H., 1957. Bodenerosion und Auelehmbildung in Deutschland. Deutsche Gewässerkundl Mitteilungen 1, 110–114.Google Scholar
Modderman, P.J.R., 1976. Abschwemmung und neolitische Siedlungsplätze in Niederbayern, Archäologisches Korrespondenzblatt 6, 105–108.Google Scholar
Natermann, E., 1941. Das Sinken der Wasserstände der Weser und ihr Zusammenhang mit der Auelehmbildung des Wesertales. Arch. L.-u. Volkskde. Niedersachsen 2, 288–309.Google Scholar
Orzechowski, S., 2007. Zaplecze osadnicze i podstawy surowcowe starożytnego hutnictwa świętokrzyskiego. Kieleckie Towarzystwo Naukowe, Kielce.Google Scholar
Pastre, J.F., Cecchini, M., Dietrich, A., Fontugne, M., Gauthier, A., Kuzucuoglu, C., Leroyer, C., Limondin, N., 1991. L’évolution Holocene des fonds de vallées au Nord-Est de la région parisienne (France). Physio-Géo 22/23, 109–115Google Scholar
Poser, H.J., Tricard, J., 1950. Terrasses et phenomenes periglaciaires dans la vallee de l'Huisne en amont du Mans (Sarthe). Bulletin de la Société Géologique de France S5-XX, nos. 7–9, 381–391.CrossRefGoogle Scholar
Przepióra, P., 2021. Subatlantyckie przemiany zlewni Kamionki na Wyżynie Kieleckiej. In: Kalicki, T. (Ed.), Monografie: Geografia i Geoarcheologia Tom I. Ośrodek Badań Europy Środkowo-Wschodniej, Kielce-Białystok, p. 97.Google Scholar
Przepióra, P., Kalicki, T., Aksamit, M., Aksamit, P., Fularczyk, K., Kusztal, P., Houbrechts, G., 2021. An macro- and microslags delta deposition of postindustrial water reservoir in Sielpia (Holy Cross Mts., Poland). In: Cunha, P., Fontana, A., Panin, A. (Eds.), FLAG 2021 Abstract Book. Institute of Geography Russian Academy of Sciences, Moscow, pp. 57–59. http://eg.igras.ru/wp-content/uploads/2021/09/Aksamit-1.pdf.Google Scholar
Przepióra, P., Kalicki, T., Chwałek, S., Houbrechts, G., 2019. Historyczny układ hydrotechniczny w Jędrowie (województwo świętokrzyskie) zachowany w formach i osadach – studium geoarcheologiczno-konserwatorskie. Acta Universitatis Lodziensis, Folia Geographica Physica 18, 5–16.Google Scholar
Przepióra, P., Kalicki, T., Houbrechts, G., 2022b. Makro- i mikrożużle w aluwiach równiny zalewowej Kamionkikoło Jędrowa (Góry Świętokrzyskie) jako wskaźnik dawnej działalności metalurgicznej. Landform Analysis 41, 69–83.CrossRefGoogle Scholar
Przepióra, P., Kalicki, T., Houbrechts, G., 2022a. The historical metallurgical activity recorded in alluvium of small river valley: case study from Kamionka River (Holy Cross Mts., Central Poland). In: Kalicki, T. (Ed.), Conference of Environmental Archaeology 2022: “The Environment as an Archive of Past Human Activities,” Kielce-Suchedniów, Abstracts, pp. 101–105.Google Scholar
Przychodni, A., 2002. Ośrodek starożytnej metalurgii żelaza nad Nidą, In: Orzechowski, S. (Ed.), Hutnictwo świętokrzyskie oraz inne centra i ośrodki starożytnego hutnictwa żelaza na ziemiach polskich. Świętokrzyskie Stowarzyszenie Dziedzictwa Przemysłowego w Kielcach, Kielce, pp. 45–60.Google Scholar
Przychodni, A., 2006. Starożytne hutnictwo nad Nidą, jako potencjalna enklawa świętokrzyskiego centrum dymarskiego. In: Orzechowski, S., Suliga, I. (Eds.), 50 lat badań nad starożytnym hutnictwem świętokrzyskim. Archeologia–Metalurgia–Edukacja. Kieleckie Towarzystwo Naukowe, Kielce, pp. 103–123.Google Scholar
Radwan, M.W., 1963. Rudy, kuźnice i huty żelaza w Polsce. Wydawnictwa Naukowo-Techniczne, Warszawa.Google Scholar
Reichelt, G., 1953. Ober den Stand der Auelehmforschung in Deutschland. Petermanns Geographische Mitteilungen 97, 245–261.Google Scholar
Richardeau, C., 1977. Distribution des sphèrules magnèticues provenant de la sidèrurgie liègeoise. dans Bulletin de la Société Géographique de Liège 13, 155–165.Google Scholar
Richling, A., Solon, J., Macias, A., Balon, J., Borzyszkowski, J., Kistowski, M. (Eds.) 2021. Regionalna Geografia Fizyczna Polski. Bogucki Wydawnictwo Naukowe, Poznań.Google Scholar
Rubinowski, Z., 1992. Główny obszar starożytnego hutnictwa żelaza w Górach Świętokrzyskich. Na podstawie wyników inwentaryzacji Bielenina K., Orzechowskiego Sz. oraz Wichmana T. (1950–1990). [Data from sketch map and typescript.]Google Scholar
Rutkowski, J., 1991. Holocen doliny dolnej Racławki. Kwartalnik AGH, Geologia 17, 173–191.Google Scholar
Rutkowski, J., Alexandrowicz, S.W., Pazdur, A., 1988. The source of the Holocene sedimentation in the lower Racławka valley. Excursion Guide Book Symposium “Lateglacial and Holocene Environmental Changes—Vistula Basin 1988,” 15–21 June 1988, Cracow, pp. 110–115.Google Scholar
Schirmer, W., 1973. The Holocene of the former periglacial areas. Eiszeitalter und Gegenwart 23/24, 306–320.Google Scholar
Schirmer, W., 1995. Valley bottoms in the Late Quaternary. In: Hagedorn, J. (Ed.), Late Quaternary and Present-Day Fluvial Processes in Central Europe. Zeitschrift f. Geomorphologie, Supplementband 100, 27–51.Google Scholar
Śliwa, A., 2007. Hydrologiczne podstawy projektu. In: Kloss, A., Kurzelewski, J. (Eds.), Zbiornik wodny Wióry. Hydroprojekt Warszawa, Oficyna Wydawnicza Sadyba, Warszawa.Google Scholar
Solon, J., Borzyszkowski, J., Bidłasik, M., Richling, A., Badora, K., Balon, J., Brzezińska-Wójcik, T., et al., 2018. Physico-geographical mesoregions of Poland: Verification and adjustment of boundaries on the basis of contemporary spatial data. Geographia Polonica 91, 143–170.CrossRefGoogle Scholar
Suliga, J., 1995. Historyczne budowle wodno-energetyczne dorzecza Kamiennej i ocena możliwości budowy nowych elektrowni wodnych. Studia i Materiały, Studium historyczne przyrodniczo-kulturowe doliny rzeki Kamiennej, Krajobrazy 8, no. 20.Google Scholar
Suligowski, R., Kupczyk, E., Kasprzyk, A., Koślacz, R., 2009. Woda w środowisku przyrodniczym województwa świętokrzyskiego. Wydawnictwo Instytutu Geografii, Jan Kochanowski University, Kielce.Google Scholar
Wróblewski, T., Wróblewska, E., 1996. Góry Świętokrzyskie, Mapa geologiczno—krajoznawcza w skali 1:200 000. Państwowy Instytut Geologiczny, Warszawa.Google Scholar
Zandstra, K.J., 1954. Die Jung Quartäre morphologische Entwicklung des Saartales. Erdkunde 8, 276–285.CrossRefGoogle Scholar
Zieliński, J., 1965. Staropolskie Zagłębie Przemysłowe. Kieleckie Towarzystwo Naukowe–Zakład Narodowy im. Ossolińskich, Wrocław–Warszawa–Kraków.Google Scholar
Figure 0

Figure 1. Location of the study area within a sketch map of the Europe (inset). The Świślina drainage basin (blue limit) and research area (red box) are shown on the Świętokrzyskie Voivodship Digital Elevation Model (DEM; created by M. Frączek on the basis of data obtained from CODGiK, MGGP Aero, no. GI-FOTO.703.44.2014) with physicogeographic mesoregions (1–3) of Poland in the catchment area (Kondracki, 1977, 2002): 1, Suchedniów Plateau (342.36); 2, Holy Cross Mountains (342.34-35); 3, Sandomierz Upland (342.36).

Figure 1

Figure 2. Geological structure of the Świślina catchment near the study site (red box) based on Detailed Geological Map of Poland 1:50,000, sheet Słupia Nowa(Filonowicz, 1966; www.pgi.gov.pl).

Figure 2

Figure 3. The Old-Polish Industrial District (OPID) border based on M. Radwan's map (Bielenin, 1992), with updated bloomery activity areas based on A. Przychodni (2002). Study site location is in the Świślina catchment area (adapted by P. Przepióra).

Figure 3

Figure 4. Study area on the Digital Elevation Model (DEM) showing profile locations (red arrows), borders of the terrace and floodplain levels (red dotted line), and loess upland (orange dotted line) (www.geoportal.gov.pl).

Figure 4

Figure 5. The K1 and K2 profiles of the Świślina terrace at Doły Biskupie (Klatka, 1958; adapted by Ł. Podrzycki and P. Przepióra).

Figure 5

Figure 6. View of the study site towards the river (left) and the location of the DB1 profile (photo by T. Kalicki 2014).

Figure 6

Figure 7. DB1 grain-size profile with Folk and Ward (1957) grain size–distribution parameters; CaCO3 content; sediment pH; concentrations of selected elements (Cu, Zn, Pb, Mn, Fe); and the microslag content in magnetic spherules per 10 g of matter (ms/10 g) with the probable level where sediment accumulation began after the period of metallurgical activity (red, dashed line).

Figure 7

Figure 8. The main area of ancient iron metallurgy in the Holy Cross Mountains based on the 1950–1990 inventory results of K. Bielenin, Sz. Orzechowski, and T. Wichman (adapted by Rubinowski [1992], and later by P. Przepióra).