As human impact have been increasing strongly over the last decades, it is crucial to distinguish human-induced dust sources from natural ones in order to define the boundary of a newly proposed epoch - the Anthropocene. Here, we track anthropogenic signatures and natural geochemical anomalies in the Mukhrino peatland, Western Siberia. Human activity was recorded there from cal AD 1958 (±6). Anthropogenic spheroidal aluminosilicates clearly identify the beginning of industrial development and are proposed as a new indicator of the Anthropocene. In cal AD 1963 (±5), greatly elevated dust deposition and an increase in REE serve to show that the geochemistry of elements in the peat can be evidence of nuclear weapon testing; such constituted an enormous force blowing soil dust into the atmosphere. Among the natural dust sources, minor signals of dryness and of the Tunguska cosmic body (TCB) impact were noted. The TCB impact was indirectly confirmed by an unusual occurrence of mullite in the peat.
Ombrotrophic peatlands are a well-known trap of atmospheric dust, trace elements and pollutants1,2,3,4 originating from both natural sources (wild fires, volcanic eruptions, dust storms, meteorite impacts)5,6,7,8 and anthropogenic sources (industry, mine, transport, nuclear tests)1,9,10,11,12,13. Knowledge about past pollution in Russia is very limited as no high-resolution peat profile of past pollution, or annual flux of trace elements and dust, has been undertaken to date.
The Siberian peatlands, one of the largest in Russia, are exceptionally interesting to explore for past geochemical signals because of their distance from any important pollution source. They are a sensitive receptor of global changes in atmospheric-dust deposition. Studies of the geochemistry of Siberian peatlands have focused predominantly on the probable impact site of the Tunguska Cosmic Body or on the pollution related to Tomsk- and Norilsk heavy industry (Fig. 1)14,15,16. Furthermore, no existing studies identify the recently proposed Anthropocene period, the period in which human activity dramatically altered all earth systems17,18,19. Here, we provide a first high-resolution record of dust flux as evidence for geochemical anomalies of both anthropogenic- and natural origin in the Mukhrino peatland in Western Siberia (Fig. 1). The Mukhrino is located over 1000 km from any large industrial center (Norilsk, Chelabinsk, Barnaul; Fig. 1). The developing oil industry in the nearest town (20 km; Khanty-Mansiysk) with a population below 100,000, seems to have a limited significance in the present context. The long distance from power plants, the ombrotrophy, the high-resolution record of palaeoecological changes all make Mukhrino a suitable place to assess human impact and the extent of airborne-particle migration – and to potentially define the boundary of the Anthropocene.
Results and Discussion
The human influence on the amount and composition of atmospheric dust deposited on Mukhrino peatland can be seen to start in the late 1950 s (Figs 2 and 3). Since then, epsilon Nd values are less negative (−6.7; −7.1) compared to those from lower layers of the peat core and 87Sr/86Sr values are less radiogenic (0.70999 ± 0.000009 − 0.710269 ± 0.000017) (Table 1, Fig. 2). Less negative epsilon Nd values and lower 87Sr/86Sr values in modern Chinese dust is ascribed by Li et al.20 as due to possible addition of anthropogenic particles. Unfortunately, values of Nd and Sr isotopes of anthropogenic material from Russia are not available. Looking into shift in values of epsilon Nd and 87S/86Sr ratio after cal AD 1953 (±7) (Fig. 2) we can hypothesized, that it is the anthropogenic impact. In the layer dated cal AD 1958 (±6), the first spheroidal aluminosilicate particles (SAP) appear and remain throughout the younger part of the profile, directly confirming the addition of technogenic particles to the deposited dust (Fig. 3). This is linked with the appearance of other chronomarkers, e.g., spheroidal carbonaceous particles (SCP), whose numbers have rapidly increased everywhere after the second world war19. SAP are a typical inorganic, glassy component of fly ash generated during industrial coal combustion21,22,23,24,25 and are found even in regions located far from industrial centres, e.g., Greenland (Summit area)26 and the glaciers of Tianshan27. Ranging in size from <1 up to tens of micrometers, the majority are ideal spheres, monolithic, and dense, porous or hollow. They result from the softening, melting and vitrification of minerals such as clays, chlorite, feldspars, etc., during coal combustion in power stations21. Although a wide compositional variation is reported for these spherical fly-ash particles23, it is the SiO2 and Al2O3 rich varieties that are mainly encountered in peatlands; these are highly resistant to dissolution28,29. EDS spectra of individual SAP in the Mukhrino peat confirm SiO2 and Al2O3 as the main components, with addition of Na, K, Mg, Ti and Fe. Particles of <9 μm (average diameter 2.7 μm; n = 120) confirm a distant source for the industrial dust28,30.
The dust flux, derived from the lithogenic, conservative element scandium, varies in the peat profile from 1–12.4 g m−2 y−1 (Fig. 2). The dust deposition rate shows a dramatic increase immediately after the first SAP appearance, reaching a maximum in cal AD 1963 (±5), and falling again soon after cal AD 1966 (±5). Atmospheric weapon testing was likely the main reason for what was the highest dust flux recorded during the last 800 years, a flux unrelated to any changes in water level at that time (Fig. 2). In cal AD 1963 (±5), the maximum value of the REE accumulation rate (AR) (SmAR – 0.13 g m−2 y−1; Fig. 2) and a maximum enrichment of U (EFU – 1.65; Fig. 3) is especially notable. This finding is in line with the observed peak in concentration of La, Th and U, and increased activities of 238Pu and 137Cs, in a peat layer dated cal AD 1963 in peatlands of the Tomsk region15 as well with maximum of above ground nuclear tests in Russia (AD 1962)31. The most powerful nuclear test was Tsar Bomba detonated at Novaya Ziemlya in 196132. Conversely, decreasing enrichment factors for Cu, Ni and Zn reflect the insignificance of pollution from heavy industry at that time in Mukhrino (Fig. 3). These observations further strengthen the point that nuclear tests were the reason for the first human-induced increase in dust fallout in Western Siberia. Here we show that nuclear tests not only caused the release of radionuclides, but also affected geochemical cycles of many elements, especially REE, and accelerated dust deposition.
Metals crucial for the Siberia region, i.e., Cu and Ni, exploited and processed in Norilsk and Tomsk, show constant enrichment-factor values (52–95 and 1.7–4.4, respectively; Fig. 3) in the period cal AD 1953 (±5) −1996 (±2). Small fluctuations in uranium might indicate minor influence of coal combustion or use of crude oil. A more obvious rise in the input of several metals (Ti, Cu, Ni, and Zn) is observed as late as in the year cal AD 2000 (±2) (Fig. 3). The increase of Ti dust flux at that time (Fig. 2) can be linked to the intensification of industrial activities in AD 2000. Lower enrichments of Zn, Cu in cal AD 1990 (±2) correspond to the fact that the economic system was weakened by a set of reforms during that time (Perestroika)33,34. Only in the Khanty-Mansi Autonomous District in AD 1998–2003 did emission increase by a factor of two and oil production by 37%33.
A depth to water table (DWT) reconstruction based on testate amoebae35 shows that dry conditions dominated up to cal AD 1750 (±62), with a maximum at the turn of 15th and 16th centuries (Fig. 2). This was followed by low carbon accumulation rates (CAR), declined signature of epsilon Nd (−8,5) and elevated 87Sr/86Sr (0.712061 ± 0.000010), similar to the signature of Chinese loess (Table 1; Sr and Nd isotopic data not available for Siberian loess). The supply of loess to dust is supported also by a characteristic value of Th/U equal 2.7–2.9, similar to the value described for loess ≈ 2.836. The decline in DWT can be associated with the Little Ice Age, consistent with climatic estimations conducted for central- and eastern Europe, and with the pattern of CAR across the Northern Hemisphere and southern Siberia37. A slight increase in dust deposition rates (Fig. 2), and a higher charcoal content (Fig. 4) correlate with the lowest water level in the peatland, and confirm the natural inforce of dryness as a driver of dust generation.
The time of abrupt change in CAR (from 22.3–244 g m−2 y−1), dust flux and several other proxies are noted in the modelled age of the 57–58 cm layer (cal AD 1882 ± 43–1920 ± 28) and is in good agreement with the date of the Tunguska cosmic body event (TCB) which happened in June 1908 (Fig. 2) and is the best known and most mysterious extra-terrestrial event recorded in Central Russia; the amount of cosmic material dispersed into the atmosphere has been estimated at ca 1 million tons38,39.
Indirect evidence of TCB-induced dust fallout in the Mukhrino peatland is an unusual occurrence of mullite in the “Tunguska layer” and its absence in adjacent layers (Supplementary Table 2). Mullite is a high-temperature phase that forms due to the decomposition and transformation of clay minerals at temperatures >1100 °C40. The mineral, together with microspherules, scoria like objects (SLOs) and other high temperature minerals (corundum, suessite) lacking in the ‘Tunguska layer’, has been deemed evidence of a Younger Dryas meteorite impact41. In the ‘Tunguska layer’, mullite may be a product of melting of dust and soil minerals at extremely high temperatures induced by the TCB explosion. A distinct peak in microscopic charcoal contents (Fig. 4), indicative of distant fires, has been recorded in this layer together with an increased concentration of Se (Supplementary Table 1), a biogenic element released during forest fires42. It is known that the TCB impact set 2000 km2 of taiga on fire. The main stream of dust formed during the TCB explosion passed westwards through Siberia, Europe and America7. As to the best of our knowledge, there were no local fires during this time in the vicinity of the Mukhrino peatland, it is proposed that post TCB fires could have influenced the dust flux and the element concentration in this peat layer. The layer is characterised by the highest Th/U value (3.9; Supplementary Table 1) which would indicate a change in the supply of natural dust.
Our reconstruction of changes in the flux and composition of dust recorded in a Siberian peat profile is an important contribution to the global discussion about the boundary of the Anthropocene and the markers defining this new geological period.
The remote location of the Mukhrino peatland makes it a valuable record of natural- and anthropogenic dust sources, and especially for the differentiation of new markers of anthropogenic activity.
Prior to cal AD 1901(±37), the supply of dust was climatically driven in the main. Then, an abrupt increase of REE, a rise of microcharcoal concentrations and the occurrence of natural mullite is indicative of the influence of theTunguska Cosmic Body impact on dust influx.
The occurrence of spheroidal aluminosilicates (SAP) from cal AD 1958 (±6) onwards is clear evidence of technogenic particles in the dust supply; anthropogenic activities were, from then on, an additional source of dust. Our results show SAP occurrence in remote places and offer important evidence to recent discussion about Global Stratotype Section and Point43,44. In considerations of a Global Standard Stratigraphic Age, as spheroidal aluminosilicates are resistant in peaty- and soil environments and easy to distinguish, they may constitute, together with SCP an unambiguous global marker of the industry-induced epoch.
The influence of Siberian heavy industry on dust geochemistry has been observed as late as cal AD 2000 (±2), when economic development considerably increased after the Perestroika-related stagnancy.
Nuclear weapons tests had the main influence on REE in the Mukhrino peat profile. In Siberia, the year cal AD 1963 (±5) is marked by the highest dust input to the peat record. In addition to the release of radionuclides, the accumulation rate and enrichment of REE can be an important indicator defining nuclear tests as drivers of increased atmospheric dust.
The Mukhrino mire is located about 20 km from Khanty-Mansiysk (60°54′N, 68°42′E) on the eastern bank of the Irtysh River in the middle taiga area of Western Siberia. A detailed site description is given in Lamentowicz et al.35 and Kremenetski et al.45. In summer 2012, a 1 m peat core was collected, sliced into 1-cm samples and divided into subsamples for various analyses. Biotic proxies (pollen analysis, macrofossil analysis, testate amoebae analysis), bulk density, ash content, charcoal and chronology, described in Lamentowicz et al.35, show the hydrological dynamics, vegetation changes and fire history of the Siberia region. In this study, we used Sr and Nd isotopes, geochemistry, mineralogy and charcoal analysis combined with the published chronology based on C14 age-depth model (cal AD y ± σ) and depth to water table (DWT)35 to reveal changes in dust flux, composition and sources.
To assess levels of pollution, 33 dry peat samples (1 g) were determined by epithermal neutron activation analysis (ENAA) for 38 main elements and REE (Supplementary Table 1). ENAA was performed at the pulsed fast reactor IBR-2 at the Frank Laboratory of Neutron Physics, JINR, Dubna, Russia. Characteristics of the neutron flux density in the two irradiation channels (one cadmium-screened) equipped with the pneumatic system and registration of gamma spectra are given elsewhere46. The gamma-spectra of the induced activity were processed using software developed in the Frank Laboratory of Neutron Physics47. Pelleted samples with masses of ca 0.3 g were heat-sealed in polyethylene foil bags for short-time irradiation and in aluminum cups for long-time irradiation. To determine medium- and long lived isotopes, namely, Na, Sc, Cr, Fe, Co, Ni, Zn, As, Se, Rb, Sr, Zr, Mo, Ag, Cd, Sb, Cs, Ba, La, Ce, Nd, Sm, Hf, Ta, W, Au, Hg, Th and U, cadmium-screened channel 1 at a resonance neutron fluency rate of 3.31 × 1012 n cm−2 s−1 was used. Samples were irradiated for 100 hours, repacked and, using high purity germanium detectors, measured twice after 4–5 days and 20–23 days of decay. Measurement times were 45 min and 2 hours, respectively. To determine the short-lived isotopes Mg, Al, Cl, K, Ca, Ti, V, Mn, Br, In and I, irradiation channel 2 with a thermal neutron fluency rate of 1.6 × 1013 n cm−2 s−1was used. Samples were irradiated for 3 min and measured twice after 3–5 min and 20 min of decay for 3 min and 9–10 min, respectively. Element contents were determined on the basis of certified reference materials and flux comparators47. Quality was assured by use of the Certified reference material IAEA-336 (Lichen), and NIST Standard reference materials 1632c (SRM Trace Elements in Coal (bitominous), 2710 (Highly Elevated Trace Element Concentrations (Montana Soil) and BCR (EU Community Bureau of Reference 667 (estuarine Sediment) which were irradiated simultaneously with the studied peat samples. Results were obtained with high precision and acceptable accuracy (from 3 to 15%). High precision – reproducibility of quality controls over long periods of time (years) is often better than 2% relative standard deviation (RSD).
For normalization, enrichment factors were calculated using Sc as a conservative element and reference values for the upper continental crust48. Element accumulation rates (g cm−2 y−1) were calculated according to the formula: element concentration* bulk density* peat accumulation rate. Dust flux (g m−2 y−1) was calculated according to the formula: (element concentration (Sc, Ti)/concentration of element in Upper Continental Crust)* bulk density *peat accumulation rate*1000049. Results are detailed in Supplementary Table 1.
To identify the sources of dust, the sizes, morphologies and chemical compositions of dust particles in peat samples were analyzed using Philips XL 30 ESEM and FESEM ZEISS SUPRA 35 scanning electron microscopes, both equipped with an energy dispersive system (EDS). A small portion of peat sample (~0.25 cm3) was air dried, gently homogenized, fixed to a carbon tab and carbon coated. Both backscattered electron (BSE) images carrying compositional information and secondary-electron (SE) images showing particle morphologies and shapes were used. BSE images enabled easy detection of all inorganic particles as they appear lighter in the dark background of peat organic matter29. XRD data of ashed peat samples (550 °C overnight; washed in 1 M HCl for 15 min) were obtained using a Panalytical X’Pert PRO MPD PW 3040/60 equipped with Theta-Theta geometry. Quantitative determination of crystalline phases was done by Rietveld refinement of powder diffraction data (HighScore + software). The XRD results are given in Supplementary Table 2.
Sr and Nd isotopes
To trace the sources of atmospheric dust, 143Nd/144Nd and 87Sr/86Sr values were determined in the Isotope Laboratory at UAM. About 1 gram of peat powder was burned at 550 °C overnight. Ash was dissolved on a hot plate (~100 °C for three days) in closed PFA vials using a mixture of concentrated hydrofluoric- and nitric acids (4:1). Miniaturized chromatographic techniques described by Pin et al.50 were applied for Nd and Sr separation, using some modifications in column size and reagent concentrations introduced by Dopieralska51. Strontium was loaded with a TaCl5 activator on a single Re filament, whereas Nd were measured in a Re double-filament configuration. Sr and Nd were analyzed in dynamic collection mode on a Finnigan MAT 261 mass spectrometer.
During the course of this study, the AMES standard yielded 143Nd/144Nd = 0.512129 ± 7 (2σ mean on twenty-four analyses). The NBS 987 Sr standard gave 87Sr/86Sr of 0.710230 ± 10 (2σ mean on twenty-two analyses). 87Sr/86Sr values were normalized to 86Sr/88Sr = 0.1194 and 143Nd/144Nd values to 146Nd/144Nd = 0.7219. Total procedure blanks were less than 35 pg for Nd and Sm, and less than 80 pg for Sr. Epsilon Nd (εNd) was calculated using standard formula: εNd sample = (143/144Ndsample-0,512638)/0,512638)*10000. The data are given in Table 1.
Microscopic charcoal was used as a proxy for regional fire activity (mainly frequency)52,53 and macroscopic charcoal to reconstruct local fires54,55. Microscopic charcoal analysis was carried out for the entire length of the profile. Samples were prepared following standard procedures for pollen analysis with addition of Lycopodium tablet as an indicator of concentration56,57. Microscopic charcoal particles (>10 μm) were counted as by Tinner and Hou58 and Finsinger and Tinner59. In the 50–64 cm section of the core, macroscopic charcoal analysis (particles > 100 μm; 1 cm3 peat samples), followed the method of Whitlock and Larsen60. Microscopic- and macroscopic charcoal accumulation rates (CHARmicro, CHARmacro; particles/cm2/yr) were calculated using the charcoal concentrations (CHACmicro, CHACmacro) and peat accumulation rates inferred from the age-depth model.
How to cite this article: Fiałkiewicz-Kozieł, B. et al. Anthropogenic- and natural sources of dust in peatland during the Anthropocene. Sci. Rep. 6, 38731; doi: 10.1038/srep38731 (2016).
Publisher's note: Springer Nature remains neutral with regard to jurisdictional claims in published maps and institutional affiliations.
Shotyk, W. History of atmospheric lead deposition since 12,370 14C yr BP recorded in a peat bog profile, Jura Mountains, Switzerland. Science 281, 1635–1640 (1998).
Le Roux, G. et al. Volcano- and climate-driven changes in atmospheric dust sources and fluxes since the Late Glacial in Central Europe. Geology 40(4), 335–338 (2012).
Vanneste, H. et al. Late-glacial elevated dust deposition linked to westerly wind shifts in southern South America. Scientific Reports 5, 11670 (2015).
Fiałkiewicz-Kozieł, B. et al. Peatland Microbial Communities as Indicators of the Extreme Atmospheric Dust Deposition. Water Air Soil Pollution 226 (2015).
Nriagu, J. O. A global assessment of natural sources of atmospheric trace metals. Nature 338, 47–49 (1989).
Gladysheva, O. G. On the problem of the Tunguska meteorite material. Solar System Research. 41, 314–321 (2007).
Kusky, T. Asteroids and meteorites: Catastrophic collisions with Earth. The hazardous Earth (2009).
Vanneste, H. et al. Elevated dust deposition in Tierra del Fuego (Chile) resulting from Neoglacial Darwin Cordillera glacier fluctuations. Journal of Quaternary Science 31(7), 713–722 (2016).
Turco, R. P. et al. Nuclear winter: global consequences of multiple nuclear explosions. Science 222, 1283–1292 (1983).
Nriagu, J. O. & Pacyna, J. M. Quantitative assessment of worldwide contamination of air, water and soils by trace metals. Nature 333, 134–139 (1988).
De Vleeschouwer, F. et al. Anthropogenic impacts in North Poland over the last 1300 years - A record of Pb, Zn, Cu, Ni and S in an ombrotrophic peat bog. The Science of the Total Environment 407(21), 5674–5684 (2009).
Allan, M. et al. Mid- and late Holocene dust deposition in Western Europe: The Misten peat bog (Hautes Fagnes – Belgium). Climate of the Past 9, 2285–2298 (2013).
Baklanov, A. A. et al. Aspects of atmospheric pollution in Siberia. In: Regional Environmental Changes in Siberia and Their Global Consequences. Groisman, P. Y., Gutman, G. (Eds.). 303–346 (2013).
Tositti, M. et al. A multitracer study of peat profiles from Tunguska, Siberia. Global and Planetary Change 53, 278–289 (2006).
Mezhibor, A., Arbuzov, S., Rikhvanov, L. & Gauthier-Lafaye, F. History of the Pollution in Tomsk Region (Siberia, Russia) According to the Study of High-Moor Peat Formations. International Journal of Geosciences 2, 493–501 (2011).
Stepanova, V. A. et al. Elemental composition of peat profiles in western Siberia: Effect of the micro-landscape, latitude position and permafrost coverage. Applied Geochemistry 53, 53–70 (2015).
Crutzen, P. J. & Stoemer, E. F. The “Anthropocene”. IGBP Newsletter 41, 17–18 (2000).
Ellis, E. C., Fuller, D. Q., Kaplan, J. O. & Lutters, W. G. Dating the Anthropocene: Towards an empirical global history of human transformation of the terrestrial biosphere. Elementa: Science of the Anthropocene 1, 000018 (2013).
Swindles, G. T. Spheroidal carbonaceous particles are a defining stratigraphic marker for the Anthropocene. Scientific Reports 5, 10264 (2015).
Li, G., Chen, J., Ji, J., Yang, J. & Conway, T. M. Natural and anthropogenic sources of East Asian dust. Geology 37(8), 727–730 (2009).
Vassilev, S. V. & Vassileva, C. G. Mineralogy of combustion wastes from coal-fired power stations. Fuel Processing Technology 47, 261–280 (1996).
Sokol, E. V., Maksimova, N. V., Volkova, N. I., Nigmatulina, E. N. & Frenkel, A. E. Hollow silicate microspheres from fly ashes of the Chelyabinsk brown coals (South Urals, Russia). Fuel Processing Technology 67, 35–52 (2006).
Giere, R., Carleton, L. E. & Lumpkin, G. R. Micro- and nanochemistry of fly ash from a coal-fired power plant. American Mineralogist 88, 1853–1865 (2003).
Goodarzi, F. Morphology and chemistry of fine particles emitted from a Canadian coal-fired power plant. Fuel 85, 273–280 (2006).
Kutchko, B. G. & Kim, A. G. Fly ash characterization by SEM-EDS. Fuel 85, 2537–2544 (2006).
Drab, E., Gaudichet, A., Jaffrezo, J. L. & Colin, J. L. Mineral particles content in recent snow at Summit (Greenland). Atmospheric Environment 36, 5365–5376 (2002).
Zhang, X. L., Wu, G. J., Yao, T. D., Zhang, C. L. & Yue, Y. H. Characterization of individual fly ash particles in surface snow at Urumqi Glacier No. 1, Eastern Tianshan. Chinese Science Bulletin 56, 3464–3473 (2011).
Smieja-Król, B. & Fiałkiewicz-Kozieł, B. Quantitative determination of minerals and anthropogenic particles in some Polish peat occurrences using a novel SEM point-counting method. Environmental Monitoring and Assessment 186, 2573–2587 (2014).
Smieja-Król, B., Fiałkiewicz-Kozieł, B., Sikorski, J. & Palowski, B. Heavy metal behavior in peat - a mineralogical perspective. The Science of the Total Environment 408, 5924–5931 (2010).
Lawrence, C. R. & Neff, J. C. The contemporary physical and chemical flux of aeolian dust: A synthesis of direct measurements of dust deposition. Chemical Geology 267, 46–63 (2009).
Nagdy, M. & Rosen, M. Nuclear Weapons. https://ourworldindata.org/nuclear-weapons/ (2016).
Khalturin, V. I., Rautian, T. G., Richards, P. G. & Leith, W. S. A Review of Nuclear Testing by the Soviet Union at Novaya Zemlya, 1955–1990. Science and Global Security 13(1), 1–42 (2005).
Bityukova, V. R. Dynamic of atmospheric pollution by stationary sources. Regional research of Russia 1, 394–398 (2011).
Cooper, J. The Russian economy twenty years after the end of the socialist economic system. Journal of Eurasian Studies 4, 55–64 (2013).
Lamentowicz, M. et al. Hydrological dynamics and fire history of the last 1300 years in western Siberia reconstructed from a high-resolution, ombrotrophic peat archive. Quaternary Research 84, 312–325 (2015).
Gallet, S., Jahn, B. M., Lanoe, B. V., Dia, A. & Rossello, E. Loess geochemistry and its implications for particle origin and composition of the upper continental crust. Earth and Planetary Science Letters 156(3–4), 157–172 (1998).
Hildebrandt, S. et al. Tracing the North Atlantic decadal-scale climate variability in a late Holocene pollen record from southern Siberia. Palaeogeography, Palaeoclimatology, Palaeoecology 426, 75–84 (2015).
Bronshten, V. A. The Nature of the Tunguska Meteorite. Meteoritics & Planetary Science 34, 723–728 (1999).
Xie, L. W., Hou, Q. L., Kolesnikov, E. M. & Kolesnikova, N. V. Geochemical Evidence for the Characteristics of the 1908 Tunguska Explosion Body in Siberia, Russia. Science in China (Ser. D) 44, 1029–1037 (2011).
Castelein, O., Guinebretiere, R., Bonnet, J. P. & Blanchart, P. Shape, size and composition of mullite nanocrystals from a rapidly sintered kaolin. Journal of the European Ceramic Society 21, 2369–2376 (2001).
Bunch, T. E. et al. Very high-temperature impact melt products as evidence for cosmic airbursts and impacts 12,900 years ago. Proceedings of the National Academy of Sciences of the United States of America 109, E1903–E1912 (2012).
Samsonov, Y. N. Particulate emissions from fires in central Siberian Scots pine forests. Canadian Journal of Forest Research 35, 2207–2217 (2005).
Lewis, S. L. & Maslin M. A. Defining the Anthropocene. Nature 519, 171–180 (2015).
Waters, C. N. et al. The Anthropocene is functionally and stratigraphically distinct from the Holocene. Science 351 (2016).
Kremenetski, K. V. et al. Peatlands of the Western Siberian lowlands: current knowledge on zonation, carbon content and Late Quaternary history. Quaternary Science Reviews 22, 703–723 (2003).
Frontasyeva, M. V. Neutron activation analysis for the Life Sciences. A review. Physics of Particles and Nuclei 42(2), 332–378 (2011).
Pavlov, S. S., Dmitriev, A. Yu. & Frontasyeva, M. V. Automation system for neutron activation analysis at the reactor IBR-2, Frank Laboratory of Neutron Physics, Joint Institute for Nuclear Research, Dubna, Russia. Journal of Radioanalytical and Nuclear Chemistry, doi: 10.1007/s10967-016-4864-8 in press (2016).
Rudnick, R. L. & Gao, S. Composition of the Continental Crust. In: Treatise on Geochemistry. Holland, H. D. & Turekian, K. K. (Editors) Elsevier, Amsterdam. 3, 1–64 (2004).
Fagel, N. et al. Deciphering human-climate interactions in an ombrotrophic peat record: REE, Nd and Pb isotope signatures of dust supplies over the last 2500 years (Misten bog, Belgium). Geochimica et Cosmochimica Acta 135, 288–306 (2014).
Pin, Ch., D., Briot, Ch., Bassin & Poitrasson, F. Concomitant separation of strontium and samarium-neodymium for isotopic analysis in silicate samples, based on specific extraction chromatography. Analytica Chimica Acta 298, 209–222 (1994).
Dopieralska, J. Neodymium isotopic composition of conodonts as a palaeoceanographic proxy in the Variscan oceanic system, Ph.D. thesis, pp. 111, Justus-Liebig-University, Giessen (2003).
Tinner, W. et al. Pollen and charcoal in lake sediments compared with historically documented forest fires in southern Switzerland since AD 1920. The Holocene 8, 31–42 (1998).
Gardner, J. J. & Whitlock, C. Charcoal accumulation following a recent fire in the Cascade Range, northwestern USA, and its relevance for fire-history studies. The Holocene 11, 541–549 (2001).
Clark, J. S. Stratigraphic charcoal analysis on petrographic thin sections: application to fire history in northwestern Minnesota. Quaternary Research 30, 81–91 (1988).
Conedera, M. et al. Reconstructing past fire regimes: methods, applications, and relevance to fire management and conservation. Quaternary Science Reviews 28, 555–576 (2009).
Stockmarr, J. Tablets with spores used in absolute pollen analysis. Pollen et Spores 13, 615–621 (1971).
Berglund, B. E. & Ralska-Jasiewiczowa, M. Pollen analysis and pollen diagrams. In: Handbook of Holocene Paleoecology and Paleohydrology ed. Berglund BE (Chichester-Toronto: Wiley & Sons Ltd.) pp. 455–484 (1986).
Tinner, W. & Hu, F. S. Size parameters, size-class distribution and area-number relationship of microscopic charcoal: relevance for fire reconstruction. The Holocene 13, 499–505 (2003).
Finsinger, W. & Tinner, W. Minimum count sums for charcoal-concentration estimates in pollen slides: accuracy and potential errors. The Holocene 15, 293–297 (2005).
Whitlock, C. & Larse, C. Charcoal as a fire proxy., Tracking environmental change using lake sediments. Terrestrial, algal, and siliceous indicators. Eds Smol, J. P., Birks, H. J. B. & Last, W. M. (Kluwer, Dordrecht) pp. 75–97 (2001).
Lightfoot, P. C. et al. Remobilisation of continental lithosphere by a mantle plume: major-, trace – element, and Sr-, Nd-, Pb- isotope evidence from picritic and tholeiitic lavas of the Noril’sk District, Siberian Trap, Russia. Contributions to Mineralogy and Petrology 114, 171–188 (1993).
Podkovyrov, V. N. et al. Provenance and Source Rocks of Riphean Sandstones in the Uchur–Maya Region (East Siberia): Implications of Geochemical Data and Sm–Nd Isotopic Systematics. Stratigraphy and Geological Correlation 15(1), 41–56 (2007).
Chen, J. et al. Nd and Sr isotopic characteristics of Chinese deserts: Implications for the provenances of Asian dust. Geochimica et Cosmochimica Acta 71, 3904–3914 (2007).
Rao, W. et al. Nd-Sr isotope geochemistry of fine-grained sands in the basin-type deserts, West China: Implications for the source mechanism and atmospheric transport. Geomorphology 246, 458–471 (2015).
Yasnyginaa, T. A. et al. The ICP-MS Determination of Rare Earths and Other Metals in Baikal Crude Oil: Comparison with Crude Oils in Siberia and the Russian Far East. Doklady Earth Sciences 411(8), 1237–1240 (2006).
Hart, S. R., Blusztajn, J., Dick, H. J. B., Meyer, P. S. & Muehlenbachs, K. The fingerprint of seawater circulation in a 500-meter section of ocean crust gabbros. Geochimica et Cosmochimica Acta 63, 4059–4080 (1999).
Esser, B. K. & Turekian, K. K. The Osmium isotopic composition of the continental crust. Geochimica et Cosmochimica Acta 57, 3093–3104 (1993).
The research was funded by grant 2011/01/D/ST10/02579 from the Polish National Centre of Science (NCN) (PI: Barbara Fiałkiewicz-Kozieł). We acknowledge the support of the International Network for Terrestrial Research and Monitoring in the Arctic (INTERACT) that funded the project: “Functioning of Siberian mire ecosystems and their response to climate changes” (CliMireSiber) (PI: Fatima Laggoun-Defarge) and Grant PSPB-013/2010 through the Swiss Contribution to the enlarged European Union (CLIMPEAT, www.climpeat.pl) (PI: Mariusz Lamentowicz). This study is a contribution to the Virtual Institute of Integrated Climate and Landscape Evolution (ICLEA) of the Helmholtz Association and Science and Research Funds for 2015–2016, allocated to a co-financed international project (No. 3500/ICLEA/15/2016/0). We thank Dr Mirosława Pawlyta for SEM help and dr Tomasz Krzykawski for XRD analyses. Professor Richard Hoover (Athens State University, Alabama, USA) and Dr. Padraig Kennan (University College Dublin, Ireland) are thanked for discussion and language improvement. We also wish to thank Dr Francois de Vleeschouwer, Dr. Gaël Le Roux (ECOLAB, Université de Toulouse, CNRS, INPT, UPS, Toulouse, France) and Prof. Zdzisław Bełka (UAM, Poznań, Poland) for discussion.
The authors declare no competing financial interests.
Electronic supplementary material
Rights and permissions
This work is licensed under a Creative Commons Attribution 4.0 International License. The images or other third party material in this article are included in the article’s Creative Commons license, unless indicated otherwise in the credit line; if the material is not included under the Creative Commons license, users will need to obtain permission from the license holder to reproduce the material. To view a copy of this license, visit http://creativecommons.org/licenses/by/4.0/
About this article
Cite this article
Fiałkiewicz-Kozieł, B., Smieja-Król, B., Frontasyeva, M. et al. Anthropogenic- and natural sources of dust in peatland during the Anthropocene. Sci Rep 6, 38731 (2016). https://doi.org/10.1038/srep38731
This article is cited by
Anthropogenic impacts in the Changbai Mountain region of NE China over the last 150 years: geochemical records of peat and altitude effects
Environmental Science and Pollution Research (2019)
By submitting a comment you agree to abide by our Terms and Community Guidelines. If you find something abusive or that does not comply with our terms or guidelines please flag it as inappropriate.