Trace Metals and Diatom Stratigraphy along the Sill between Lakes Telaga Warna and Telaga Pengilon, Dieng, Central Java, Indonesia

: This study examines the spatiotemporal variations in diatom assemblages and selected metal concentrations (Pb, Cr, Cd, Al, and Zn) in bed sediments of lakes Telaga Pengilon and Telaga Warna in Dieng, Indonesia to document natural and/or anthropogenic changes in the local aquatic and terrestrial environment. The analyses focused on sediments collected from a 150-cm core taken from a sill between the two lakes, which exhibit signiﬁcant differences in water chemistry. The core was subdivided into 14 stratigraphic intervals allowing for an analysis of the vertical (and temporal) variations in diatom composition and selected metal concentrations. A total of 103 taxa from 25 genera were identiﬁed in the core. Diatom assemblages were dominated by Eunotia (56%), Pinnularia (17.2%), and Frustulia (4.6%). The most abundant species was Eunotia, a diatom that can tolerate a wide range of pH conditions. Given that pH within waters of the two lakes differs signiﬁcantly, the abundance of Eunotia suggests that pH in the area between Telaga Pengilon and Telaga Warna varied through time, potentially ranging from about 2.5 to 8. Changes in pH were likely related to alterations in hydrological conditions. Metal concentrations varied with depth/time of deposition within the core. Peak metal concentrations appear to be related to the inﬂux of debris from a volcanic eruption. Based on the principle component analysis (PCA), the input of volcanic materials also inﬂuenced diatom assemblages and resulted in a distinct layer of broken diatom frustules. Relatively low metal concentrations in surface sediments suggest that the erosion of hillslope soils in response to agricultural activity did not signiﬁcantly impact the lakes.


Introduction
Indonesia is an archipelago that has 130 active volcanos, including those associated with the Dieng plateau, a plateau located about 2100 m above sea level within the regencies of Wonosobo and Banjarnegara. Many of the volcanic craters in the Dieng plateau have a history of explosive eruptions that have led to the significant loss of human life [1,2].
Lakes within the Dieng plateau, including lakes Telaga Warna and Telaga Pengilon, have primarily been produced by the collapse of volcanic calderas following eruptions that released massive amounts of lava, volcanic ash, and rocks. Once formed, these depressions are rapidly filled by rainfall and runoff associated with Indonesia's humid tropical climate [1,3].
Telaga Pengilon and Telaga Warna are both small lakes that have become particularly significant tourist destinations, and the area has been named a conservation area due to the presence of several endemic species, including Alcedinidae, Ictinaetus malayanensis and diversity to be used to assess changes in water quality and other environmental conditions [23][24][25].
In this study, diatoms from a long-term core extracted from the sill between lakes Telaga Warna and Telaga Pengilon, were used in conjunction with environmental variables to investigate the effects of selected heavy metal on the diatom community structure. Inherent in the approach was: (1) An analysis of the temporal changes in the composition and biodiversity of benthic diatoms in the area between Telaga Warna and Telaga Pengilon, (2) a temporal analysis of the variations in the influx of selected metals to the lakes, and (3) an interpretation of the potential causes of variation in environmental conductions during the deposition of the sill's upper 1.5 m of sediment.

Study Area
The Dieng plateau, located in Wonosobo, Central Java, is located about 2096 m above sea level. The elongate, northwest-southeast trending plateau is approximately 14 km long and 6 km wide. Climatically, it is characterized by a humid, wet, subtropical climate. The average annual rainfall is 2652 mm, most of the precipitation falls between November and March. The average daily temperatures are relatively constant (~14 • C), but can reach values near 0 • C during the dry season. Geologically, it is underlain by a variety of rock types, including limestones, tuffaceous sandstones, and volcanic assemblages, including basalts and basaltic andesite. Geomorphologically, the Dieng plateau is a volcanically hazardous and complex landscape consisting of late Quaternary to recent volcanic stratocones, vents and craters, the more recent features possess a history of recurrent phreatic eruptions and the emission of poisonous gases [26,27]. The prominent volcanic features are associated with the Dieng volcanic complex which consists of late Quaternary to recent volcanic deposits.
Lakes in Dieng, in general, are formed in volcanic craters with a relatively high acidity caused by the influx of volcanic gases, and high concentrations of magnetic volatiles, such as SO 2 , H 2 S, HCl, and HF. Lake Telaga Warna is a representative example, and is currently enriched (134 to 240 ppm) in dry gas (up to 90% H 2 O and lesser amounts of CO 2 , SO 2 , and SO 4 ) and around 1.6 ppm H 2 S [2,28]. These constituents have created acidic, extremely low pH conditions that are exacerbated by evaporation during periods of limited rainfall. In contrast, lake Telaga Pengilon generally exhibits a pH of around 6 and possesses a high concentration of minerals. However, pH is influenced and varies in response to significant precipitation during the 6-month rainy season.
The area along the corridor between lakes Telaga Warna and Telaga Pengilon was selected as a study area (Figure 1), in part, since it was considered representative of a relatively undisturbed area within the plateau. In comparison to other lakes on the plateau, agriculture is relatively limited within the lake basin. The study focuses on a sediment core that was extracted from the divide (or sill) between the two lakes. The sill is characterized by hydrologic conditions characterized by shallow water, about 1-2 m deep during the wet season, surrounded by an undulating terrain covered with Actinoscirpus grossus (a grass) and other macrophytes.
A small channel traverses the sill and hydrologically connects the two lakes, at least during the rainy season. Water along the corridor (sill) is composed of a mixture of both acidic and slightly alkaline to neutral waters derived from both lakes Telaga Warna and Telaga Pengilon, respectively. During the rainy season, the area is completely flooded as a result of increased water volumes from both lakes, and flooding is expected to influence the rate of diatom growth. The average annual water temperature at the site was 21.5 • C, whereas the elevation of the sill is about 2088 masl.

Sediment and Core Collection
A sediment core from the wetland between the two lakes was obtained using a manual coring device near the mid-point of the divide (sill) and within the deepest part of the wetland area (07°12.904′ S, 109°54.894′ E). The extracted core was 150 cm long. Upon collection, the core was described and subsequently sampled at approximately 10 cm intervals for diatom and geochemical analyses.

Diatom and Geochemical Analyses
Once in the laboratory, the sediment samples were allowed to air dry for 3 days before they were digested to extract the diatoms. All diatom samples were oxidized following a procedure modified from Battarbee et al. [29] and outlined in Soeprobowati et al. [3]. The procedure involved the hot acid digestion of the sediments with 10% HCL and 10% H2O2, during which time the sample was heated for 2 h at >80 °C. Following digestion, the sample was washed with distilled water. This process was repeated three times, after which the samples were allowed to sit overnight to allow the natant to be effectively separated from the supernatants (the acidic solution could be removed). Washing of the sediment was then repeated several times until its pH was neutral.
A microscopic slide of the sample was prepared using an evaporation procedure in which 400 µL was dropped on the coverslip. It was then dried on the hotplate and mounted to the slide with Naphrax. Identification of the diatoms was performed using a light microscope at 1000 magnification, and a minimum of 400 diatom valves was enumerated and counted [5]. Diatom taxonomy for species followed the methods put forth by [30][31][32][33][34][35][36][37][38][39], and were checked in the Algabase.org database [40].
Sediment samples were analyzed for selected metals, including lead (Pb), cadmium (Cd), chromium (Cr), zinc (Zn), and aluminum (Al). The four trace metals (Pb, Cd, Cr, and Zn) were selected as they are commonly abundant in volcanic rocks, and (in the case of Zn) it was associated with the utilized agricultural fertilizers. Aluminum is one of the most abundant naturally-occurring metals, and is often wide spread in the environment. However, it was analyzed here since it is enriched in the B-and C-horizon of the upland tropical soils in the form of oxides and hydroxides. Thus, when combined with its generally low solubility under normal pH and Eh conditions and its association with clay minerals, it was thought to serve as a potential tracer of eroded upland soils.
The selected metals were analyzed using a slightly modified version of USEPA Method 200.7. This multi-step analysis involved the digestion of 200 mg of dried and homogenized sediment, <2 mm in size, in 125 mL polypropylene screw-top bottles containing 4 mL of aqua regia (3:1 HNO3 to HCl). The bottles were sealed and held at 90 °C in a water bath for 60 min. The leaches were then transferred to 100 mL volumetric flasks and

Sediment and Core Collection
A sediment core from the wetland between the two lakes was obtained using a manual coring device near the mid-point of the divide (sill) and within the deepest part of the wetland area (07 • 12.904 S, 109 • 54.894 E). The extracted core was 150 cm long. Upon collection, the core was described and subsequently sampled at approximately 10 cm intervals for diatom and geochemical analyses.

Diatom and Geochemical Analyses
Once in the laboratory, the sediment samples were allowed to air dry for 3 days before they were digested to extract the diatoms. All diatom samples were oxidized following a procedure modified from Battarbee et al. [29] and outlined in Soeprobowati et al. [3]. The procedure involved the hot acid digestion of the sediments with 10% HCL and 10% H 2 O 2 , during which time the sample was heated for 2 h at >80 • C. Following digestion, the sample was washed with distilled water. This process was repeated three times, after which the samples were allowed to sit overnight to allow the natant to be effectively separated from the supernatants (the acidic solution could be removed). Washing of the sediment was then repeated several times until its pH was neutral.
A microscopic slide of the sample was prepared using an evaporation procedure in which 400 µL was dropped on the coverslip. It was then dried on the hotplate and mounted to the slide with Naphrax. Identification of the diatoms was performed using a light microscope at 1000 magnification, and a minimum of 400 diatom valves was enumerated and counted [5]. Diatom taxonomy for species followed the methods put forth by [30][31][32][33][34][35][36][37][38][39], and were checked in the Algabase.org database [40].
Sediment samples were analyzed for selected metals, including lead (Pb), cadmium (Cd), chromium (Cr), zinc (Zn), and aluminum (Al). The four trace metals (Pb, Cd, Cr, and Zn) were selected as they are commonly abundant in volcanic rocks, and (in the case of Zn) it was associated with the utilized agricultural fertilizers. Aluminum is one of the most abundant naturally-occurring metals, and is often wide spread in the environment. However, it was analyzed here since it is enriched in the B-and C-horizon of the upland tropical soils in the form of oxides and hydroxides. Thus, when combined with its generally low solubility under normal pH and Eh conditions and its association with clay minerals, it was thought to serve as a potential tracer of eroded upland soils.
The selected metals were analyzed using a slightly modified version of USEPA Method 200.7. This multi-step analysis involved the digestion of 200 mg of dried and homogenized sediment, <2 mm in size, in 125 mL polypropylene screw-top bottles containing 4 mL of aqua regia (3:1 HNO 3 to HCl). The bottles were sealed and held at 90 • C in a water bath for 60 min. The leaches were then transferred to 100 mL volumetric flasks and brought up to volume with ultra-pure deionized water. The samples were analyzed by Inductively Coupled plasma optical emission spectroscopy (ICP-OES) (Perkin Elmer Optima 4100DV ICP-OES) on the campus of Western Carolina University (USA). The platform was calibrated with USGS standard reference materials GXR-1, GXR-2, and GXR-5 and NIST standard reference materials 2709 and 2711. Along with a reagent blank, the analyte concentrations for these five SRMs were plotted against blank-subtracted integrated peak areas. A regression line was fitted to the calibration points and the equation of the line was used to quantify unknown sample concentrations. Deviation of standards from this regression line was used to estimate analytical accuracy, replicate analyses were used to determine analytical precision, and analyses of reagent blanks are used to estimate lower limits of detection. Precision and accuracy were generally within +/−5%.

Data Analysis
Environmental and diatom data were analyzed using different multivariate methods. Species with a relative abundance of <2% were removed from the statistical analysis. The diatom assemblage was graphed using the software package C2 version 1.7.7 [41]. Diatom data were transformed as log(x + 1) to stabilize the variance, and tested for normality. The principal component analysis (PCA) was conducted to identify the major environmental variables that influenced the data set, and to determine the relationship between metal variables and diatom species. In addition, Pearson correlation analyses (p < 0.05 and p < 0.01 levels) were also conducted on the five metals (Pb, Cd, Cr, Zn, and Al). These analyses were performed using the RStudio software [42]. The hierarchical cluster analysis was applied using the unweighted pair group method with an arithmetic mean (UPGMA) [43]. The results show diatom zones based on assemblages with similar Bray Curtis similarity species as analyzed using PAST version 3.1.5 [44].

Vertical Distribution of Diatoms
A total of 103 different species of diatoms belonging to 25 genera were recorded in 14 samples from the core. There were 11 dominant taxa that exceeded a 2% relative abundance, the threshold was required to be included in the statistical analyses. A large group of diatoms, especially genus Eunotia, comprised approximately 56% of the total diatom community, whereas 17.2% were comprised of Pinnularia, and 4.7% of Frustulia. In general, Eunotia formica (Ehrenberg) was the dominant diatom within nearly all strata, exhibiting an abundance of 25%. Eunotia monodon var. tropica (Lange-Bertalot) comprised 20.97% of the total diatom assemblages. A cluster analysis was performed on those species that comprised more than 2% of the total. The analysis subdivided the strata in the sediment core into four diatom zones ( Figure 2).

Zone II (110-96 cm)
Zone II is characterized by poor, but variable diatom preservation between the sediment layers. Diatom frustules were abundant and well preserved in the upper layer, while at a depth below 102 cm the diatom valves were highly broken. Only broken frustule of E. monodon var. tropica (Lange-Bertalot) and E. formica (Ehrenberg) were found.

Zone III (96-60 cm)
Zone III (96-60 cm) is dominated by E. formica (Ehrenberg), Pinnularia viridiformis (Nitzsch), and Pinnularia viridis (Nitzsch). The abundance of Achanthes increased by about 6%, whereas Fragillaria and Aulacoseira increased above the abundances observed in the previous zones (below). The high abundance of Eunotia and periphytic species in the middle of the core also indicates a higher water level associated with higher pH conditions. Eunotia has the ability to respond to pH and some Eunotia have been found in the extremely acidic conditions.

Variations in Metal Concentrations
In general, Al, Cd, Pb, and Zn concentrations were relatively high at the bottom of diatom Zone I. Their concentrations decreased in the middle of Zone I, before reaching maximum concentrations at the top of Zone I and the bottom of Zone II. Concentrations of these metals then decreased sharply at the top of diatom Zone II (Figure 2). Zinc and Cd concentrations remained low through the remainder of Zones III and IV, whereas Cr and Al concentrations increased slightly before declining towards the surface. Lead also increased slightly at the top of Zone I and bottom of Zone II, before remaining relatively constant through the remainder of the core. Zn was the only metal to show an increase in the surface sediments, although the increase was limited (Figure 2).
The relationships between the metals in the 14 subsamples of the core were analyzed using the principal component analysis (PCA) (Figure 3). The first three principal components (PCs) explained 80.35% of the total variance. Component 1 explained up to 41.14% of the total variance and was characterized by high loadings of Cd (0.55) and Cr (0.51). Component 2 explained 22.79% of the total variance and was dominated by weighted values for Zn (0.58) and Pb (0.28), particularly at a depth of 66 cm (diatom Zone I). Most of the subsamples were located in the opposite quadrant from Cd and Cr (Figure 4), which were concentrated at a depth of 144 cm.

Correlation between Diatom Assemblages and Metal Concentrations
The spatial relationships between the metals within the core were exam means of Pearson's correlation analysis (Figure 3). Pearson's correlation was also highlight the relationship between the total abundance of diatoms and the enviro parameters. Statistically significant correlations were observed between Cr and 0.58, p < 0.01) Zn and Al (r = 0.55, p < 0.01) and between Cd and Al (r = 0.47, p < 0 correlation between Cd and Cr declined in diatom Zones 3 and 4 (towards the su shown in Figure 4.

Correlation between Diatom Assemblages and Metal Concentrations
The spatial relationships between the metals within the core were examined by means of Pearson's correlation analysis (Figure 3). Pearson's correlation was also used to highlight the relationship between the total abundance of diatoms and the environmental parameters. Statistically significant correlations were observed between Cr and Cd (r = 0.58, p < 0.01) Zn and Al (r = 0.55, p < 0.01) and between Cd and Al (r = 0.47, p < 0.01). The correlation between Cd and Cr declined in diatom Zones 3 and 4 (towards the surface) as shown in Figure 4.
Diatom species and environmental variables were analyzed using Pearson's correlation, where a significant correlation at level p < 0.05 was observed among most of the environmental variables and diatom species. Chromium significantly correlated with F. saxonica (0.56) but negatively correlated with P. hemipteriformis (−0.56) and P. viridiformis (−0.64). Zinc correlated significantly with E. subarcuoides (0.66) and Pinnularia Gibba (0.579). Strong and significant correlations were also observed between most diatom species. E. subarcoides significantly correlated with E. minor, both of which have greater linkages to pH and have similar auto-ecology preferences.

Implications of Spatiotemporal Variations in Diatoms
The abundance and species of diatoms varied vertically, and therefore through time, within the 150-cm core. Acidophilous and epiphytic diatom species, mainly from the genera Eunotia (28 taxa) and Pinnularia (17 species), were mostly associated with peat samples in the core, although not present in every sample. Overall, the sediment core was characterized by diatoms that are tolerant of a wide range of pH conditions. Changes in pH may be caused, in part, by seasonal variations in the delivery of alkaline waters to the acidic lake, thereby neutralizing the water's pH. Therefore, hydrological changes in the water body can temporarily become neutral or acidic, resulting in vertical variations in diatom species in the lake core. The abundances of Eunotia, in fact, can be used as an indicator of pH fluctuations (Table 1). In addition, the expansion of acidophilous taxa such as Eunotia paludosa and acidobiontic species such as Eunotia exigua (found in Lake Telaga Pengilon) become common at pH values less than 5.5. As the pH drops to 4.5 these taxa begin to replace acidophilous taxa in the assemblage. Benthic and epiphytic diatoms were also present, and are general indicators of the water level.
Signs of acidification within the core occur in the lower most sediments of the core (diatom Zone I) and the surface layer (0 cm), both of which are dominated mostly with acidophilus taxa. In general, changes in Zone I were characterized by planktonic diatom that can tolerate pH values of 5.8 that decreased in response to a decrease in pH. Acidification below a pH 5.5 led to the decline in species indicators of circumneutral water, such as Achnanthes Cymbella, Pinnularia microstauron, and Navicula hemansoides.
In Indonesia, previous studies have reported E. monodon var. tropica (Lange-Bertalot) from Lake Toba (Sumatra) [45], Borneo (Kalimantan) [46], and Papua [47]. In addition, Glushchenko and Kulikovskiy [48] reported E. monodon var. tropica (Lange-Bertalot) in southeastern Vietnam. The abundance of this species is generally regarded as an indicator of warm temperatures. Indonesia is considered a suitable environment due to the high average temperature conditions needed for E. monodon var. tropica, whereas the abundance of B. brebissonii (Ross) may indicate variations in pH at the coring site.
In contrast, Zone III was dominated by E. formica (Ehrenberg), a periphytic species that can tolerate acidic conditions (i.e., a pH range between 4.7 to 7.3) [49,50], but which is mostly characterized by neutral to slightly alkaline diatoms. Thus, diatom species in Zone III are indicators of both dystrophic and oligotrophic lake conditions, with an optimal pH of around 6.7. The increasing number of periphytic taxa in the sediments of Zone III is likely to indicate a concurrent increase and expansion of aquatic plants close to the core site, and an increase in shade caused by the plant cover [47,51].
Zone IV, was dominated with Eunotia and has been found in the acidic environment of lake Telaga Pengilon, characterized by a pH of less than 3.5. Data from this study shows that the diatom composition in the top sediment was dominated with species Eunotia bilunaris var. linearis, Eunotia muchopila, Eunotia curvata, Eunotia paludosa, Eunotia tropica, Eunotia incisa. Table 1. Diatom species reported from Telaga Pengilon with a pH of less than 3.5 (the pH range was collected from the reference by Denicola [52]).

Species pH (Range) Species pH (Range)
Achanthes In combination, these data are suggestive of relatively high water levels during the deposition of Zone III, although seasonal variations that induced short-term variations in pH were likely (as indicated by the presence of low pH tolerant species, Table 1). We believe that these variations primarily reflect (1) variations in inter-annual precipitation and evaporation which are known to influence pH in the lakes, and (2) water levels in the lakes, particularly high levels that allow hydrologic communication between the lakes via the small channel that traverses the sill. During high water levels, not only does pH increase, but the pH of lake Telaga Warna is moderated by the dilutional effects of the near-neutral conditions observed in lake Telaga Pengilon. Moreover, during high water levels, the sill area is transformed into a wetland-like area. Put differently, diatoms at the core site appear to reflect the combined variations in water levels and pH throughout the entire depositional period.
The diatoms at the bottom of Zone II are characterized by broken frustules. Broken frustules are generally caused by dissolution and physical fragmentation. In this case, the vertical contrast in the nature of the frustules (intact vs. broken) between Zone II and the overlying and underlying zones could be due to differences in the depositional environment and or source of the diatoms. More specifically, we hypothesize that the diatom valves were fragmented by the volcanic activity, the broken frustule caused by their abrasion with volcanic sand-sized grains transported and deposited in the lake. There could also be time for frustules to partially dissolve in the water column prior to settling in the layer at a depth of 102 cm.
Similar strata containing broken frustules were found in Rawa Danau (West Java, Indonesia) at a depth of around 50-125 cm, which dated to ca. 181-80 years B.P. [57]. In this case, water levels in the lake decreased, thereby initiating pedogenesis. In addition, the volcanic activity significantly changed the composition and influx of sediment and broke the diatom frustule apart within this stratigraphic layer. Research by [45], who conducted a biostratigraphic study at lakes Telaga Cebong and Telaga Balekambang near lake Telaga Pengilon, found tephra in the strata located at a depth of 477-478 cm. These sediments were also devoid of pollen. In combination, the data are suggestive of volcanic activity in the Dieng plateau that correlated with the deposition of lower Zone II sediments. Dieng has, in fact, a history of intermittent, geologically recent, volcanic eruptions. There have been 31 eruptions in Dieng during the Holocene, at least eight of which caused fatalities. The historical eruptions that occurred within the Dieng plateau have been dominated by phreatic eruptions and the emission of poisonous gases since 1375. In 1786, ground fissuring destroyed the village of Jamping killing 38 people. Eruptions in 1826 and 1827 caused several fatalities [45]. Further eruptions occurred in 1944, 1945, 1964, 1979, 2003, 2009, and 2017. The eruption of Sinila crater in 1979 included CO 2 emissions, whereas the 1979 eruption of Timbang crater included high concentrations of CO 2 and a volcanic induced earthquake. The lethal volcanic gases occurred when magma passed through a weaker zone of faulting and was trapped by a clayed layer of an altered ash pyroclastic fall deposit [58].
Supporting the above hypothesis is the occurrence of species that are suggestive of an increase in lake nutrients associated with vegetation following the deposition [59] of the lower Zone II sediments. Fragillaria in Zone III, for example, has commonly been recognized as pioneering taxa and represents a successional stage that frequently follows an eruption.

Spatiotemporal Variations in Metals
Lake bed sediments commonly serve as significant sinks for both major and trace metals, and have been extensively used to assess variations in contaminant loadings to lacustrine systems, particularly from anthropogenic sources [60]. In this study, three sources of Cd, Cr, Pb, and Zn were initially hypothesized: (1) The potential influx of metals from hydrothermal zones of mineralization, (2) sediments from volcanic eruptions, and (3) the erosion of hillslope soils, particularly in response to recent agricultural activity, which may have been amended by Zn containing fertilizers.
Pearson's correlation analysis of the metals, combined with the PCA, suggests that in the lower deposits (diatom Zones I and II), Cd and Cr, and to a lesser degree, Pb and Zn were derived from a similar source. Both Pb and Zn are commonly associated with one another in hydrothermal ore bodies, and Cd often follows Zn in these types of geological materials. In addition, water-rock interactions under acidic conditions may enrich rockderived elements in lake bed sediments, including, for example, those examined herein [61]. It is interesting to note, however, that all four elements exhibited maximum concentrations at the top of Zone I and within the bottom sediments of Zone II ( Figure 2). As noted above, the diatoms in Zone II were characterized by broken frustules, suggestive of a volcanic eruption. Thus, we believe that the increase in metal concentrations is reflective of the input of volcanic materials to the lake from an eruption during the deposition of upper Zone I and lower Zone II sediments. Figure 2, and the PCA, show that spatial variations between Cd, Cr, Zn, and Pb differ between Zones I/II and Zones III/IV. These differences may reflect changes in the predominant source(s) of the metals. Inputs from hillslope erosion were postulated as a possible source of the metals. The erosion rates in the Dieng plateau in general are very high, exceeding 480 tons/ha/year and are exacerbated by high intensity rainfall during the rainy season. The total rainfall in the region ranges between 2500-3500 mm/year in the Dieng plateau [62,63]. However, the agricultural activity within the Telaga Warna and Telaga Pengilon lake basins has remained limited to date, suggesting that the impacts of hillslope erosion on lake water and sediment quality may be relatively minor.
Aluminum was analyzed here as a potential indicator of hillslope erosion as Al oxides/hydroxides is an important component of the areas upland soils, and it is associated with clay minerals (which are abundant in the soil's B-horizon). However, Al and the other elements lacked a pronounced increase in metal concentrations towards the surface of the core, suggesting that the hillslope erosion has not had a significant effect on metal concentrations. This is consistent with the fact that there is not a lot of agriculture in the lake basin.
Conservation and forest restoration activities in the Telaga Warna and Telaga Pengilon lake basins, which uses endemic species (Altingiaceae, Burseraceae, Cannabaceae, Cunoniaceae, Ericaceae, Fagaceae, Hamamelidaceae, Juglandaceae, and Phyllanthaceae), has been going on for 3 years, from 2015-2017. During 2015, the governments performed reforestation using 85 species of tree to protect the area around Telaga Warna and Telaga Pengilon. The reforestation efforts planted 950 seedlings in an area of ±2.56 ha in order to protect Telaga Pengilon from potato farming around Dieng and to increase the vegetation cover [64].

Conclusions
This study examines the spatiotemporal distribution of diatoms and selected metals in a core extracted from a sill between two contrasting lakes, including Pb, Cd, Cr, Zn, and Al to gain sights into change in the lakes' aquatic conditions. The conclusions are summarized as follows: (1) The high abundance of acid-tolerant Eunotia species throughout the core indicate that pH fluctuated at the coring site. The observed variations in pH were presumably related to the influence of water level fluctuations at the coring site in response to both seasonal and inter-annual variations in precipitation. Variations in water levels were also likely to result in differences in the amount of hydrologic mixing between lake waters. During periods of low water, more acidic conditions characterized by minimal lake water mixing was likely. During higher water levels, pH was likely to increase, in part due to the mixing of the acidic waters in lake Telaga Warna with the higher pH waters in lake Telaga Pengilon. (2) The occurrence of diatoms with broken frustules at the bottom of Zone II with relatively high peak metal concentrations of Cd, Cr, Pb, and Zn at the top of Zone I and the bottom of Zone II suggest that lake conditions were impacted by the input of volcanic debris from a local eruption. This argument is supported by diatom assemblages found in the sediments overlying Zone II, which includes pioneering species that are known to follow eruptions in the area.
(3) Metal concentrations, including Al, did not increase towards the surface of the sediments, suggesting that recent agricultural activities and the associated impact on hillslope soil erosion has not significantly impacted the lakes. This is not surprising given that in contrast to adjacent areas, the lake basin is located in a protected conservation area that is not extensively farmed.