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Cheng Hangxin, Peng Min, Zhao Chuandong, et al. Epigenetic geochemical dynamics...
Оригинальная статья I Original article V
DOI: http://dx.doi.org/10.21285/2686-9993-2020-43-3-375-417
Epigenetic geochemical dynamics and driving mechanisms of chemical elemental distribution patterns in soil in Southwest China*
© Hangxin Chenga, Min Pengb, Chuandong Zhaoc, Wei Hand, Huiyan Wange, Qiaolin Wangf, Fan Yangg, Fugui Zhangh, Chengwen Wangi, Fei Liuj, Yalong Zhouk, Shiqi Tangl, Kuo Lim, Ke Yangn, Zheng Yango, Xiaomeng Chengp, Ziwan Chenq, Hua Zhangr, Chunhu Mos
a-pInstitute of Geophysical & Geochemical Exploration, Chinese Academy of Geological Sciences, Langfang, China bChina University of Geosciences (Beijing), Beijing, China qYunnan Institute of Geological Survey, Kunming, China 'Sichuan Geological Survey, Chengdu, China sGuizhou Geological Survey, Guiyang, China
Abstract: The Earth's surface is a complex system involving mutual interactions of its many components, including mountains, rivers, forests, farmlands, lakes and grasses. The interaction and mutual feedback of chemical elements in Earth's surface layer can drive changes in chemical elemental distribution patterns. In this study, we evaluated the mechanisms and interactions driving the distribution patterns of macroelements, probiotics, halogens and heavy metals in soils in Southwest China, based on a systematic geochemical land-quality survey at a scale of 1:250000. The results showed that the parent material determines the natural state of chemical elements in land resources. Epigenetic geochemical dynamics reshapes the distribution patterns of chemical elements in top soil; biogeochemical processes drive the evolutionary trends of land quality; and human activities, such as mining, disrupt the natural evolution of chemical elemental distribution patterns. The establishment of an epigenetic geochemical dynamics theory allows the construction of a framework for understanding the Earth's surface layer and promoting technological innovations for the comprehensive geochemical investigation of land resources.
Keywords: epigenetic geochemical dynamics, driving mechanisms, distribution pattern of elements in soils, Southwest China
Acknowledgments: During the project, more than 100 researchers and workers from the Yunnan Geological Survey, Sichuan Geological Survey and Guizhou Geological Survey participated in the field work. More than 20 researchers from the Central Laboratory of the Institute of Geophysical and Geochemical Exploration of the Chinese Academy of Geological Sciences participated in the sample analysis and testing processes. The authors would like to thank all participants for their contributions to this work.
Information about the article: Received July 08, 2020; revised August 10, 2020; accepted September 04, 2020.
For citation: Cheng Hangxin, Peng Min, Zhao Chuandong, Han Wei, Wang Huiyan, Wang Qiaolin, et al. Epigenetic geochemical dynamics and driving mechanisms of chemical elemental distribution patterns in soil in Southwest China. Nauki o Zemle i nedropol'zovanie = Earth sciences and subsoil use. 2020;43(3):375-417. (In Russ.) https://doi.org/10.21285/2686-9993-2020-43-3-375-417
* The article was provided by the Earth Science Frontiers journal within the framework of the agreement between the editorial boards of Irkutsk National Research Technical University (Irkutsk, Russia) and China University of Geosciences (Beijing, China) on the exchange of open access scientific papers.
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Earth sciences and subsoil use / ISSN 2686-9993 (print), 2686-7931 (online)
Эпигенетическая геохимическая динамика и движущие механизмы закономерностей распределения химических элементов в почвах Юга-Западного Китая*
© Хансинь Чэна, Минь Пэнь, Чуаньдун Чжаос, Вэй Ханьй, Хуйянь Ване, Цяолинь Ван', Фань Янд, Фугуй Чжан11, Чэнвэнь Ван', Фэй Лю', Ялун Чжоук, Шици Тан1, Ко Лит, Кэ Янп, Чжэн Ян0, Сяомэн Чэнр, Цзывань Чэнь^, Хуа Чжанг, Чуньху МоБ
а-рИнститут геофизических и геохимических исследований Китайской академии геологических наук, г. Ланфан, Китай ьКитайский геологический университет (Пекин), г. Пекин, Китай ^Юньнаньский институт Геологической службы, г. Куньмин, Китай гСычуаньская геологическая служба, г. Чэнду, Китай 8Геологическая служба Гуйчжоу, г. Гуйян, Китай
Резюме: Поверхность Земли представляет собой сложную систему, включающую взаимодействие многих ее компонентов, в том числе гор, рек, лесов, сельскохозяйственных угодий, озер и трав. Взаимодействие и взаимная обратная связь химических элементов в поверхностном слое Земли может привести к изменениям в структуре распределения химических элементов. В этом исследовании авторы оценили механизмы и взаимодействия, определяющие характер распределения макроэлементов, пробиотиков, галогенов и тяжелых металлов в почвах Юго -Западного Китая, на основе систематического геохимического исследования качества земли в масштабе 1:250000. Результаты показали, что исходный материал определяет естественное состояние химических элементов земельных ресурсов. Эпигенетическая геохимическая динамика меняет характер распределения химических элементов в верхнем слое почвы, биогеохимические процессы определяют эволюционные тенденции качества земли, а деятельность человека, такая как добыча полезных ископаемых, нарушает естественную эволюционную схему распределения химических элементов. Создание теории эпигенетической геохимической динамики позволяет построить основу для понимания поверхностного слоя Земли и продвигать инновационные технологии для всестороннего геохимического исследования ресурсов земной коры.
Ключевые слова: эпигенетическая геохимическая динамика, движущие механизмы, закономерности распределения элементов в почвах, Юго-Западный Китай
Благодарности: В процессе реализации проекта более ста исследователей и сотрудников из геологических служб провинций Юньнань, Сычуань и Гуйчжоу принимали участие в полевых работах. Более двадцати ученых из Центральной лаборатории Института геофизических и геохимических исследований Китайской академии геологических наук были привлечены к анализу и тестированию собранных образцов. Авторы хотели бы поблагодарить всех участников за их вклад в эту работу.
Информация о статье: Поступила в редакцию 08 июля 2020 г.; поступила после рецензирования и доработки 10 августа 2020 г.; принята к публикации 04 сентября 2020 г.
Для цитирования: Чэн Хансинь, Пэн Минь, Чжао Чуаньдун, Хань Вэй, Ван Хуйянь, Ван Цяолинь [и др.]. Эпигенетическая геохимическая динамика и движущие механизмы закономерностей распределения химических элементов в почвах Юга-Западного Китая. Науки о Земле и недропользование. 2020. Т. 43. № 3. С. 375-417. https://doi.org/10.21285/2686-9993-2020-43-3-375-417
Background
Epigenetic geochemical dynamics explores the driving mechanisms, dynamic processes, and fractionation mechanisms of the distribution, allocation, migration and evolution of chemical elements and isotopes in surface rocks, water bodies, soils, organisms, atmosphere and other media or layers of the Earth. The Earth's surface is a complex system composed of various interact-
ing components, such as mountains, water bodies, forests, farmlands, lakes and grasslands. This system controls and regulates the natural habitat and maintains the resources required to sustain life on Earth [1]. The pedosphere is the key interface, at which the lithosphere, hydrosphere, biosphere and atmosphere interact. It plays an important role in the redistribution of elements, and is also an essential interface for
* Статья была предоставлена редакцией журнала Earth Science Frontiers в рамках соглашения между редакциями Иркутского национального исследовательского технического университета (г. Иркутск, Россия) и Китайского геологического университета (г. Пекин, Китай) об обмене научными статьями открытого доступа.
Геоэкология
supporting economic and social developments [2]. Presently, the Earth is facing a serious environmental crisis in history. This has caused dysfunction in the Earth's surface layer and led to major changes in the global environment on which human survival depends. Understanding the behavior of chemical elements within the physical, chemical and biological processes of the Earth's surface, along with human-environmental interactions, has inevitably become a hot topic in exploratory geochemistry. Research in this area can reveal the driving mechanisms behind changes in the content and macroscopic distribution of elements in soil, thereby provide scientific solutions for the rational exploitation and utilization of natural resources.
In this study, we analyzed the mountainous regions near several cities including Zhaotong City in Yunnan Province, Bijie City in Guizhou Province, and Yibin and Luzhou Cities in Sichuan Province, and examined the driving mechanisms of chemical elemental distribution in soil.
Geographical and geological settings
The study area is located at the junction of Yunnan, Guizhou and Sichuan Provinces (102—
107° E and 25-30° N). The geographical environment of the area is complex, with different climate types co-existing at different elevations, and with significant regional variations. In the last 45 years, the average annual precipitation of the area was 1,885 mm, while temperature, precipitation and evaporation are increasing [3, 4].
The study area mainly consists of mountains and valleys, showing strong down-cutting and Karst landforms. The terrain slopes northwards, as behind elevation lowers gradually from the southwest to the northeast by a difference of greater than 3,400 m (Fig. 1). Farmlands, forests and grasslands accounted for 48.8 %, 41.4 % and 5.2 % of the total area of the region, respectively, and they represent the major land-use types in the region (Fig. 2).
All strata in the area have different degrees of exposure, where carbonate rocks, such as limestone and dolomite, from various periods, are widely distributed. Basalt, carbonate and sedimentary clastic rocks are the main parent materials of the regional soil (Fig. 3).
Lead (Pb), zinc (Zn) and silver (Ag) constitute the area's dominant mineral resources formed in the Devonian and Permian periods. The ores are
Fig. 1. Terrain distribution in the Zhaotong - Bijie - Yibin - Leshan - Luzhou area Рис. 1. Распределение высот рельефа в районе Чжаотун - Бицзе - Ибинь - Лэшань - Лучжоу
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Fig. 2. Land-use types in the Zhaotong - Bijie - Yibin - Leshan - Luzhou area Рис. 2. Типы землепользования в районе Чжаотун - Бицзе - Ибинь - Лэшань - Лучжоу
usually present in carbonaceous strata, comprising interbedded dolomite, dolomitic limestone, limestone and marl in the area. The area also features paragenetic or associated non-ferrous, rare and precious metal elements such as copper (Cu), iron (Fe), silver, gallium (Ga), cadmium (Cd) and germanium (Ge) [5, 6].
Basalt, carbonate and Pb-Zn-Ag deposits are mainly distributed in the mid- and high-elevation mountainous areas above 1,000 m (Fig. 3). The Emeishan large igneous province (LIP) resulted from a mantle-plume melting event spanning less than 1 Ma at approximately 259 Ma [7]. Spatially, Emeishan basalt is mainly distributed in Yunnan, Sichuan and Guizhou Provinces along the western margin of the Yangtze Craton. This region extends to Guangxi and Chongqing in the east and is bordered by the Ailaoshan - Red River fault to the west and the Longmenshan - Xiaojing River fault to the northwest. As it is near the Sanjiang tectonic belt, the Emeishan LIP's complex
geological history includes strong deformation and destructive events that resulted in approximately 0.25106 km2 exposed area. The basalt in the study area is located within the continental rift system in the Emeishan basalt zone [8], where the exposed area covered approximately 8,867 km2 (Fig. 3) or approximately 10.46 % of the total study region; while the exposed carbonate rocks covered 20,934 km2 or approximately 24.70 % of the study area.
The Geochemical Atlas of China12 and the Geochemical Survey Report of Chinese Farmland3 clear show abnormal enrichment of metal elements in the soil and stream sediments in the Emeishan basalt and the southwestern carbonate areas. These areas have high metallic elemental contents relative to elsewhere in China.
Therefore, it is essential to study the epige-netic geochemical processes in these areas and the impact of Pb and Zn mining activities on the regional elemental distribution. The findings
1 Xie X., Ren T., Sun H. Geochemical atlas of China. Beijing: Geological Publishing House, 2012. 120 p.
2 Xie X., Cheng Z., Zhang L., et al. Geochemical atlas of 76 elements in Southwest China. Beijing: Geological Publishing House, 2008. 219 p.
3 China Geological Survey. Geochemical survey report on China's cultivated land (2015). Available from: http://www.cgs.gov.cn/upload/201506/20150626/gdbg.pdf [Accessed 25 June 2015].
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Fig. 3. Distribution map of the parent materials and Pb-Zn-Ag deposits in the Zhaotong - Bijie - Yibin - Leshan - Luzhou area Рис. 3. Карта распределения материнских горных пород и месторождений Pb-Zn-Ag в районе Чжаотун - Бицзе - Ибинь - Лэшань - Лучжоу
can facilitate the advancements of the theories of epigenetic geochemical dynamics, as well as development of geochemical surveys and monitoring systems for land resources, and applications of exploratory geochemistry in natural resource management.
Data sources
The data used in this study were obtained through tests in accordance with the "Multi-Purpose Regional Geochemical Survey" specifications (1:250,000) (DZ/T 0258-2014)4. The sampling depths of the top and deep soil samples were 0-20 cm and 150-180 cm, respectively. The samples were analyzed in the Central Laboratory of the Institute of Geophysical and Geochemical Exploration, Chinese Academy of Geological Sciences. The tested elements and indicators included Ag, As, Au, B, Ba, Be, Bi, Br, Cd, Ce, Cl, Co, Cr, Cu, F, Ga, Ge, Hg, I, La, Li, Mn, Mo, N, Nb, Ni, P, Pb, Rb, S, Sb, Sc, Se, Sn, Sr,
Th, Ti, Tl, U, V, W, Y, Zn, Zr, SiO2, A^Os, TFe2Os, MgO, CaO, Na2O, K2O, TC, organic carbon (Corg) and pH. The schemes for analysis and quality control used in this study are as described in the references [9]. A quality assessment of the data, analyzed according to the prescribed procedures, showed that the data are reliable and passed the acceptance and database audits.
Mechanisms driving the macroscopic distribution of major elements
During complex physical and chemical weathering processes, soil parent materials can form in-situ residual soil. Alluvial and proluvial soils may also appear in downstream areas due to transportation and sedimentation processes when slopes and rivers are present. Deep soil is less affected by industrial and agricultural activities, in which elemental distribution is mainly controlled geologically. Typically, when there is no significant impact from human activities, the
4 Ministry of Land and Resources of the People's Republic of China. Code for multi-target regional geochemical surveys (1:250000) (DZ/T 0258-2014). Beijing: China Standard Press, 2015. 43 p.
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elemental distribution patterns of the top soil reflects that of the deep soil. However, owing to the extensive and frequent contacts between the top soil and atmosphere, water bodies, organisms or human beings, the elemental distribution patterns in soil can be considerably modified. Emeishan basalt and carbonate rocks are the two most common soil parent materials in the study area. The dynamic processes of surface erosion, transportation and sedimentation, caused by marked elevation changes and biogeochemical effects of extensive forests, are a starting point for characterizing the mechanisms driving the macroscopic distribution of elements in this region.
Main weathering and soil formation processes of basalt and carbonate rocks. Emeishan basalt is mainly composed of basic plagioclase and pyroxene minerals with some olivine, amphibole and biotite. In an epigenetic environment, the physical weathering processes drive basic feldspar (Na[AlSi3Os]-Ca[Al2Si2Os]) to fracture along the cleavage planes. Further, the chemical weathering processes cause basic feldspar decomposition, i.e., basic feldspar ^ hydromica + K+, Na+, Ca2+ ^ kaolinite (montmorillonite) + SiO2 ^ opal + gibbsite, leading to loss of K+, Na+, Ca2+ and H2SiO4. Olivine ((Mg, Fe)2SiO4) and pyroxene (Ca(Mg,Fe,Al)[Si,Al]2O6) are unstable Fe and Mg minerals that are highly susceptible to weathering. During weathering and soil formation, especially under the action of carbonic acid, Ca2+, Mg2+ and Fe2+ ions are first separated to form bicarbonates during decomposition, then dissolved in water and carried away. Under oxidation, the low-valent iron
in these minerals is oxidized to high-valent iron, orming hydrous iron oxides. These minerals remain in-situ to form red-, brown-, and hazel-colored soils.
The main mineral component of carbonate rocks is calcium carbonate. Under the long-term action of CO2-rich rainwater, calcium carbonate undergoes chemical dissolution (CaCO3 + H2O + CO2 ^ Ca2+ + 2HCO3-). Overall, 90 % of Ca2+, Mg2+ and other dissolved substances are lost due to water transportation. The remaining materials that are insoluble in acids, such as quartz, feldspar, clay and Fe and Al oxides, remain on the surface to form soil. Therefore, the time used by the carbonate rock parent materials to form soil is up to 10 times that used by other parent materials [10, 11].
Basalt is located in the continental rift system in the Emeishan basalt area. Compared to its parent rock, the soil that basalt forms was rich in Al and Fe but depleted in Ca, Mg, Na, K and Si (Table 1). During soil formation from carbonate parent materials, approximately 96 % of Ca and 52 % of Mg were lost, whereas Fe, Al, Si, K and Na were enriched by 164, 5.5, 4, 16 and 2.9 times, respectively (Table 2).
Mechanisms driving the macroscopic distribution of Fe and Al. The above-mentioned enrichment and depletion characteristics of major elements during soil formation have been clearly verified through their spatial distributions. The deep and top soils above the basalt and limestone parent materials were considerably enriched in Fe and Al, indicating significant control by soil parent materials over the distributions
Table 1. Chemical compositions of major elements in Emeishan basalt and soil
Таблица 1. Химический состав основных элементов в Эмейшанских базальтах и почвах
Statistics wb / %
SiO2 AI2O3 TFe2O3 MgO CaO Na2O K2O
Number of samples 859 859 859 859 859 859 859
Minimum 27.83 9.4 6.48 0.32 0.09 0.06 0.09
Maximum 67.47 25.39 31.41 8.73 14.04 3.2 3.5
Mean 42.17 17.16 17.4 1.14 0.73 0.39 1.08
Median 41.6 17.56 17.97 1.01 0.52 0.29 1.04
Standard deviation 6.43 2.28 3.26 0.6 0.94 0.35 0.36
Average chemical composition of the Emeishan basalt (n = 416)* 50.03 13.89 14.06 5.17 8.45 2.84 1.33
Soil / Rock 0.84 1.24 1.24 0.22 0.09 0.14 0.81
Note. * - see reference [8]. Примечание. * - см. источник [8].
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Table 2. Chemical compositions of major elements in carbonate rocks and soil Таблица 2. Химический состав основных элементов в карбонатных породах и почвах
Sampling medium Statistics wb / %
SiO2 Al2O3 TFe2O3 MgO CaO Na2O K2O
Carbonate Number of samples 34 34 34 34 34 34 34
Minimum 9.75 1.9 0.01 0.03 0.1 0.02 0.01
Maximum 96.21 4.66 0.43 7.23 55.39 0.06 1.31
Mean 16.13 2.62 0.05 0.93 48.33 0.04 0.06
Median 10.03 2.49 0.01 0.37 52.19 0.04 0.01
Standard deviation 20.34 0.48 0.1 1.43 12.89 0.01 0.23
Soil Number of samples 495 495 495 495 495 495 495
Minimum 30.72 5.88 1.79 0.13 0.12 0.05 0.17
Maximum 87.18 26.76 24.48 1.33 22.13 0.73 3.99
Mean 64.34 14.36 7.54 0.45 1.99 0.12 1.01
Median 63.99 14.24 6.81 0.43 0.37 0.09 0.78
Standard deviation 12.68 4.3 3.82 0.2 3.9 0.09 0.7
Soil / Rock 3.99 5.47 164.3 0.48 0.04 2.87 16.01
of Fe and Al (Figs. 4 and 5). Furthermore, Fe and Al contents in soil increased with elevation (Fig. 6), suggesting that during soil formation, Fe and Al did not substantially migrate from high elevations to the base of mountains. Therefore, the high Fe and Al contents in soil were the result of secondary enrichment due to parent material weathering.
The top soil is in direct contact with the atmosphere and biosphere and affected by industrial and agricultural activities. During soil formation, the soluble base cations in the top soil are more likely to be washed away, resulting in lower pH (5.82) than the deep soil (6.04). Additionally, irrespective of ground cover types (farmlands, forests, grasslands, etc.), the root system of vegetation is mainly concentrated at a shallow depth of tens of centimeters. Moreover, the root and mi-crobial growth activities of crops can produce large quantities of organic acids, adding to the already highest levels of acid rain in China the study area receives. In acidic environments, Fe2+ and Fe3+ are formed during the weathering of Fe rich ferromagnesian minerals. The migration capacity of Fe2+ is much greater than that of Fe3+, and exchangeable Al is more likely to enter the soil solution and migrates with water. Together, these factors were suggested as the main mechanism driving the lowering of TFe2O3 and Al2O3 concentrations in the top soil, in this case, by 4.6 % and 4.9 %, respectively (Fig. 6), compared to the top soil.
Mechanisms driving the macroscopic distributions of Na, K, Ca, Mg and Si, and pH. Because Na, K, Ca and Mg are soluble in water, these elements are prone to being washed away and can easily enter the epigenetic environment during weathering and soil formation. The levels of some elements such as Ca, Na (Fig. 7), K and Mg (not shown) in the top and deep soils increased rapidly with decreasing elevations (Fig. 7), suggesting that these elements mainly entered the surface water system and migrated from high- to low-elevation areas under the action of hydrodynamic forces.
Owing to their different geochemical properties, the above-mentioned elements have significantly different migration and transportation pathways after entering the epigenetic environment. Although Na and K have similar geochemical properties, the hydration energy of Na (indicating how closely the ions are surrounded by water molecules) is greater than that of K. A larger hydration energy means the ion is more difficult to be adsorbed. Therefore, in an epigenetic environment, Na is more likely to migrate with water, whereas K is more easily adsorbed by clay minerals or colloids. This is also the main reason Na was concentrated near the lowest terrain along the Yangtze River (Fig. 8, a), whereas K only occurred in low concentrations in the same area (Fig. 8, b).
Геоэкология
Fig. 4. The TFe2O3 distribution pattern in top (0-20 cm) (a) and deep (150-180 cm) (b) soils of the Zhaotong - Bijie - Yibin - Luzhou - Leshan area Рис. 4. Схема распределения TFe2O3 в верхних (0-20 см) (a) и глубоких (150-180 см) (b) почвах района Чжаотун - Бицзе - Ибинь - Лучжоу - Лэшань
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Fig. 5. The AI2O3 distribution pattern in top (0-20 cm) (a) and deep (150-180 cm) (b) soils of the Zhaotong - Bijie - Yibin - Luzhou - Leshan area Рис. 5. Схема распределения AI2O3 в верхних (0-20 см) (a) и глубоких (150-180 см) (b) почвах района Чжаотун - Бицзе - Ибинь - Лучжоу - Лэшань
Геоэкология
8
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Fig. 6. Plot of TFe2O3 (a) and AhO3 (b) contents in top and deep soils vs. elevation in the Zhaotong - Bijie - Yibin - Luzhou - Leshan area Рис. 6. График содержания TFe2O3 (a) и AhO3 (b) в верхних и глубоких почвах в зависимости от высоты в районе Чжаотун - Бицзе - Ибинь - Лучжоу - Лэшань
Fig. 7. Plot of CaO (a) and Na2O (b) contents in top and deep soils vs. elevation in the Zhaotong - Bijie - Yibin - Luzhou - Leshan area Рис. 7. График содержания CaO (a) и Na2O (b) в верхних и глубоких почвах в зависимости от высоты в районе Чжаотун - Бицзе - Ибинь - Лучжоу - Лэшань
The solubilities of sodium chloride and sodium hydroxide at room temperature were 36 g/NaCl and 109 g/NaOH in 100 g water, respectively, while that of calcium bicarbonate was 16.6 g/CaHCO3 in 100 g water. These compounds appeared mainly in the forms of Ca2+, Cl-, Na+ and OH- in natural water. As temperature rises, Ca2+ precipitates before Na2+. All Na, K, Ca and Mg were lost and enter into the water system during weathering and soil formation. However, due to solubility differences, Ca2+ and Na+, Ca and Mg (not shown) were mainly concentrated in the soils along both sides of the tributary systems, e.g, the Jinsha and Chishui Rivers, by the action of hydrodynamics (Fig. 9, a). Contrarily, Na migrated over a long distance and concentrated within the
lowest-lying areas near the Yangtze River (Fig. 8, a).
Potassium (K+), Na+, Ca2+, Mg2+ and other basic ions can all neutralize H+ and prevent and regulate the acidification of water bodies and soil. Weathering and soil formation of the widely distributed basalt and carbonate rocks provide sufficient basic ions, such as K+, Na+, Ca2+ and Mg2+, to the surface water for buffering acidity and maintaining moderately alkaline conditions in the soils along both sides of the water systems. Figure 9, b shows that soils on both sides of the Yangtze River tributaries, including the Jinsha, Hengjiang, Nanguang and Chishui Rivers, were moderately alkaline. These regions overlap precisely with the Ca rich areas, a clear indication of H+ neutralization by Ca2+ and other basic ions.
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Fig. 8. Distribution pattern of Na2O (a) and K2O (b) in the top (0-20 cm) soil of the Zhaotong - Bijie - Yibin - Luzhou - Leshan area Рис. 8. Схема распределения Na2O (a) и K2O (b) в верхних (0-20 см) почвах в районе Чжаотун - Бицзе - Ибинь - Лучжоу - Лэшань
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Fig. 9. Distribution pattern of CaO (a) and pH levels (b) in the top (0-20 cm) soil of the Zhaotong - Bijie - Yibin - Luzhou - Leshan area Рис. 9. Схема распределения CaO (a) и уровней pH (b) в верхних (0-20 см) почвах района Чжаотун - Бицзе - Ибинь - Лучжоу - Лэшань
Геоэкология
The insoluble materials formed via weathering and soil formation from carbonate rocks mainly include extremely fine-grained quartz, feldspar and clay [10, 11]. The study area has abundant annual rainfall, and the terrain exhibits strong undercutting. Silicone content increased
rapidly as elevation decreases (Fig. 10), indicating that, under the action of epigenetic hydrodynamics, insoluble minerals, such as quartz and feldspar, migrated along the water system and deposited in the lower-lying terrain in the Leshan - Yibin - Luzhou area (Fig. 11).
Fig. 10. Plot of SiO2 content in top and deep soils vs. elevation in the Zhaotong - Bijie - Yibin - Luzhou - Leshan area Рис. 10. График содержания SiO2 в верхних и глубоких почвах в зависимости от глубины в районе Чжаотун - Бицзе - Ибинь - Лучжоу - Лэшань
Fig. 11. Distribution pattern of SiÜ2 in the top (0-20 cm) soil in the Zhaotong - Bijie - Yibin - Luzhou - Leshan area Рис. 11. Схема распределения SiÜ2 в верхних (0-20 см) почвах в районе Чжаотун - Бицзе - Ибинь - Лучжоу - Лэшань
Геоэкология
Mechanism driving the macroscopic distribution of Corg, N, S and P. According to the procedures of the National Land Quality Geochemical Survey, we analyzed the levels of 52 elements, pH and Corg5. Thirty-five of the elements participate in biogeochemical processes and have clear biological effects. They included Na, K, Be, Mg, Ca, V, Cr, Mo, W, U, Mn, Fe, Co, Ni, Cu, Ag, Zn, Cd, Hg, B, Al, Tl, C, Si, Sn, Pb, N, P, As, Sb, S, Se, F, Cl and I [12]. In particular, C, N, P and S were the main elements involved in the biogeochemical cycle.
In the study area, the Corg, N, S and P contents in the top soil were significantly greater than in the deep soil. As elevation increases, the elemental contents in both soils gradually in-
creased. The absolute increase of the four elements in the top soils of the mid- and high-elevation mountainous areas above 2,000 m were significantly greater than that of the low-elevation areas (Fig. 12). In the major agricultural production region, the top soil was only slightly enriched in all four elements. Organic carbon (Fig. 13), N (Fig. 14), S and P (not shown) were significantly enriched in the top soils of the Zhaotong - Bijie forest and grassland areas above 2,000 m.
Carbohydrates, lipids, proteins and nucleic acids are the four basic substances essential for life; and C, O, H, N, P and S are the major elements required for the synthesis of these basic substances. In the biogeochemical process of plant growth, C and N are mainly involved in the
Fig. 12. Plot of Corg (a), N (b), P (c) and S (d) contents in the top and deep soils vs. elevation in the Zhaotong - Bijie - Yibin - Luzhou - Leshan area Рис. 12. График содержания Corg (a), N (b), P (c) и S (d) в верхних и глубоких почвах в зависимости от глубины в районе Чжаотун - Бицзе - Ибинь - Лучжоу - Лэшань
5 Ministry of Land and Resources of the People's Republic of China. Code for multi-target regional geochemical surveys (1:250000) (DZ/T 0258-2014). Beijing: China Standard Press, 2015. 43 p.
Геоэкология
Geoecology
Cheng Hangxin, Peng Min, Zhao Chuandong, et al. Epigenetic geochemical dynamics.
Fig. 13. Distribution pattern of Corg in the top (0-20 cm) (a) and deep (150-180 cm) (b) soils of the Zhaotong - Bijie - Yibin - Luzhou - Leshan area Рис. 13. Схема распределения Corg в верхних (0-20 см) (a) и глубоких (150-180 см) (b) почвах в районе Чжаотун - Бицзе - Ибинь - Лучжоу - Лэшань
Геоэкология
Fig. 14. Distribution pattern of N in the top (0-20 cm) (a) and deep (150-180 cm) (b) soils of the Zhaotong - Bijie - Yibin - Luzhou - Leshan area Рис. 14. Сема распределения N в верхних (0-20 см) (a) и глубоких (150-180 см) (b) почвах в районе Чжаотун - Бицзе - Ибинь - Лучжоу - Лэшань
Геоэкология
synthesis of carbohydrates and lipids, while S and P are needed to synthesize proteins and nucleic acids. Thus, the C/N ratio remains fixed in the plant body (C:N = 15). The functions of C, N, S and P render them to follow nearly identical evolutionary patterns in plant production. Although a large amount of chemical fertilizers (mainly nitrogen fertilizers) have been used in agricultural production in China in the last 30 years [13], analyses clearly demonstrate that Corg, N, S and P enrichment in the top soils of the Zhaotong - Bijie - Yibin - Luzhou - Leshan area is driven by the biogeochemical processes of forest and grassland ecosystems. Despite minor cumulation of Corg, N, S and P in the top soils of the Yibin - Luzhou - Leshan agricultural area, the accumulation effects attributed to intensive agricultural activities are significantly smaller than those naturally occurring in forest and grassland ecosystems.
Mechanism driving the macroscopic distribution of Cl, Br and I
The Cl, Br and I concentrations in the top soils of the study area were 23.3 %, 51.1 % and 23.5 %, respectively, higher than that in the deep soil; however, the F content was slightly lower in the top soil (-2.8 %).
The combined analyses of elevation variations and the F, Cl, Br and I contents in the top and deep soils showed that the F content was basically the same at different elevations, but highest at around 1,500 m above sea level, indicating that F does not change significantly with elevation in an epigenetic environment (Fig. 15, a). Hence, F concentrations showed consistent spatial distribution patterns in both soils (not shown). Moreover, F rich areas coincided with the carbonate rich areas. Fluorine distribution is mainly controlled by the carbonate parent materials.
Fluorine, Cl, Br and I are halogen elements known by their high chemical reactivity. Chlorine often exists as a monovalent anion (Cl-) as well as Cl(V) and Cl(VII) species in the natural environment. Chlorine released during soil formation is mostly in water-soluble form and eventually migrates into the ocean along with water. Therefore, the Cl contents in marine sediments or sedimentary rocks are relatively high. We found that Cl, Br and I levels in the top soil were all significantly
higher than in the deep soil. However, chlorine content increased with decreasing elevation (Fig. 15, b), indicating Cl migration from medium and high elevations to the low hilly areas, whereas Br and I contents increased with increasing elevation (Fig. 15, c,d).
The Cl distribution pattern showed that it had significantly enriched the top soils on both sides of the Yangtze River and in the Pd-Zn-Ag deposit in the Leshan - Yibin - Luzhou area (Fig. 16), consistent with extensive distribution of Cl rich carbonate rocks in the study area. Chlorine released during weathering and soil formation is concentrated along both sides of the Yangtze River, due to the action of hydrodynamic forces, and forms an ionic compound with Na. This is the primary reason we detected abnormally high levels of Cl and Na (Fig. 8, a) on both sides of the Yangtze River.
The Cl anomaly region between the Luoze and Xiaochang Rivers is near a Pd-Zn-Ag mine cluster (Fig. 3). A study on the mineral composition of the deposits found that chlorargyrite exists in the oxidation zone of the large Pb-Zn-Ag deposits in Yinchangpo, Guizhou Province [14]. The high Cl content in chlorargyrite (24.7 %) suggested that natural weathering and mining activities might have driven the high degree of Cl enrichment in the deposits.
Due to the impact of the parent materials, the deep soil above the basalt and carbonate source rocks were generally enriched in Br and I (Figs. 17, b and 18, b). In the top soil, especially in mid-alpine forests with basalt parent materials, Br and I exhibited distinct cumulative distribution patterns (Figs. 17, a and 18, a).
In the natural environment, Br and I contents in the soil are usually much higher than in the parent rocks. According to classical geochemical theories, soil Br and I are believed to mainly come from the atmosphere [15], while atmospheric Br and I originate from ocean evaporation [16]. We found the soil contents of both elements gradually increased with increasing elevation, especially above 2,000 m, indicating high mountain blockage and abundant rainfall are the main reasons for the high Br and I soil contents. Bromine and I in the natural environment mainly exist as compounds. Alpine terrain and precipitation scouring can enable iodine compounds to enter water
Геоэкология
4000
3000
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200 400 600 800
w(F)/(mg kg ')
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A
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i 0o °
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Fig. 15. Plots of F (a), Cl (b), Br (c) and I (d) contents in the top and deep soils vs. elevation in the Zhaotong - Bijie - Yibin - Luzhou - Leshan area Рис. 15. График содержания F (a), Cl (b), Br (c) и I (d) в верхних и нижних почвах в зависимости от глубины в районе Чжаотун - Бицзе - Ибинь - Лучжоу - Лэшань
systems and flow into the ocean. However, the increasing Br and I contents in the top soil of the Zhaotong - Bijie alpine valley and low Br and I contents in the soils along the Yangtze River (Fig. 15, c,d), clearly indicated that Br and I do not exist as water-soluble compounds in soil.
A literature review suggests that sediments rich in organic matter are strongly enriched with iodine; such relationship can be used to determine iodine-holding ability of soils [17]. Indeed, we found positive linear correlation between Corg and Br (R2 = 0.92) or I (R2 = 0.88) in the top soil of the study area, confirming Br and I enrichments via strong adsorption (Fig. 19). The Corg contents in mid- and high-elevation alpine forests and grasslands (Fig. 13, a) closely aligned spatially with Br and I enrichments, thus further suggested that Br and I mainly occur in their adsorbed form. Iodine is restricted to the medium and high elevation areas due to soil organic
matter adsorption, making it difficult to enter the piedmont basin. This is also the main reason for the local iodine deficiency in the piedmont basin [18].
Mechanisms driving the macroscopic distribution of heavy metals
Heavy metals are metal elements with a density of 4.5 g/cm3 or more. Of the 60 naturally occurring metal elements with atomic numbers from 23 (V) to 92 (U), fifty-four have a density greater than 4.5 g/cm3. The following 10 metals are classified as heavy metals in industrial applications: Cu, Pb, Zn, Sn, Ni, Co, Sb, Hg, Cd and Bi. Because arsenic has a toxicity similar to that of heavy metals and a density of 5.73 g/cm3, it is also included as a heavy metal when it occurs in the environment. According to the characteristics of the parent materials in the study area, we selected Pb, Zn, Cd, Ag, Cu, Ni, Co, Ti and V for our investigation and discussion.
Геоэкология
Fig. 16. Chlorine distribution pattern in the top (0-20 cm) soil of the Zhaotong - Bijie - Yibin - Luzhou - Leshan area Рис. 16. Схема распределения Cl в верхних (0-20 см) почвах в районе Чжаотун - Бицзе - Ибинь - Лучжоу - Лэшань
Lead, Zn, Cd and Ag. The study area is rich in Pb, Zn and Ag resources. Currently, more than 400 Pb-Zn deposits have been discovered, including 5 large and 14 medium-size deposits. There are 14 silver deposits (including one large and three medium-size deposits). Lead, Zn and Ag deposits are mainly distributed in the Yiliang -Hezhang, Huize - Weining and Butuo - Qiaojia mine-cluster areas. Presently, there are more than 120 Pb, Zn and Ag mines, among which 42 are in operation and the rest suspended or closed.
The distributions of Pb, Zn, Ag and Cd showed that the concentration centers of Pb (Fig. 20), Zn (Fig. 21), Ag (Fig. 22) and Cd (Fig. 23) in both top and deep soils were strictly controlled by the distributions of Pb, Zn and Ag deposits in the Pb-Zn-Ag mine clusters. Comparison of Pb, Zn, Ag and Cd levels in both soils revealed clear cumulative distribution patterns for all elements regardless of their absolute contents. Additionally, regional Pb, Zn, Ag and Cd peaks occurred in the top soils of the Weining - Hezhang area in Gui-zhou Province.
Our analyses showed that the cumulation patterns of Pb, Zn, Ag and Cd in the top soils changed with elevation. Lead, Zn and Cd contents peaked at the same elevation as the Pb, Zn and Ag deposits (Fig. 24, a-c), with decreasing Ag content as elevation declines (Fig. 24, d). Compared to deep soil, concentrations of Pb, Zn, Ag and Cd in the top soil were higher by 29.8 %, 6.8 %, 18.9 % and 169 %, respectively. The difference was more than three orders of magnitude. For Cd, its contents in the top soil were 142 %, 235 % and 102 % higher than in the deep soil at elevations below 1,800 m, 1,800-2,700 m and above 2,700 m, respectively. For Zn, meanwhile, 2,400 m was the point of division: at below 2,400 m, the Zn content in the top soil was 618 % higher than in the deep soil, and the difference grew as elevation decreases. At above 2,400 m, the differences were further reduced and even became negative at above 2,800 m. The changes in Pb and Ag concentrations in the top soil, however, were significantly different from those for Zn and Cd. As elevation decreases, Pb and Ag contents in the top soil became increasingly similar to that in the deep soil.
Геоэкология
Earth sciences and subsoil use / ISSN 2686-9993 (print), 2686-7931 (online)
Fig. 17. Bromine distribution pattern in the top (0-20 cm) (a) and deep (150-180 cm) (b) soils of the Zhaotong - Bijie - Yibin - Luzhou - Leshan area Рис. 17. Схема распределения Br в верхних (0-20 cm) (a) и глубоких (150-180 см) (b) почвах в районе Чжаотун - Бицзе - Ибинь - Лучжоу - Лэшань
Геоэкология
Fig. 18. Iodine distribution pattern in the top (0-20 cm) (a) and deep (150-180 cm) (b) soils of the Zhaotong - Bijie - Yibin - Luzhou - Leshan area Рис. 18. Схема распределения I в верхних (0-20 cm) (a) и глубоких (150-180 cm) (b) почвах в районе Чжаотун - Бицзе - Ибинь - Лучжоу - Лэшань
Геоэкология
Fig. 19. Correlation between Corg and Br (a) or I (b) in the top soil of the Zhaotong - Bijie - Yibin - Quzhou - Leshan area Рис. 19. Корреляция между Corg и Br (a) или I (b) в верхних почвах в районе Чжаотун - Бицзе - Ибинь - Лучжоу - Лэшань
In certain geographical areas, the epigenetic geochemical behavior of elements are mainly depended on their geochemical properties and organic matters, pH and clay minerals in the top soil. A partial analysis of correlations between Pd, Zn, Ag or Cd levels in soils and organic matter or pH indicated that, the main driver of the geo-chemical behavior of Ag and Pb in an epigenetic environment is organic carbon, while that for Zn and Cd is pH (Table 3). Because Ag can be strongly adsorbed and fixed by organic matter in epigenetic environments, while Zn has relatively high solubility in acidic environments, Ag enrichment (Figs. 22, a and 24, d) and Zn depletion (Figs. 21, a and 24, b) were noted in the top soils of alpine meadows and forests.
The magnitude of increasing Pb and Cd contents in the top and deep soils at the elevation of the deposits was significantly larger than that in other areas (Fig. 24, a,c). Also, we observed Cd, Pb, Zn and Ag pollution in some regions. It suggests extreme levels of human disturbance, including mining and metal extraction, at the elevation of the deposits. A detailed literature review suggested that the Hezhang - Weining region was once (over 300 years ago) a center for indigenous zinc smelting activities, in addition to the large-, medium-, and small-size Pb and Zn mines such as Tianqiao (Zhugongtang), Wuliping, Shaojiwan, Yadu and Zhushachang mines that are currently in operation or closed. The slag formed during mining has been spread throughout the region [19, 20] and is the main source of
Cd, Pb, Zn and Ag pollution (Fig. 25). In a survey of Cd contents in corn in the above-mentioned areas found that 12.1 % of the investigated corn had Pb and Cd contents higher than the allowable amounts [21]. Such finding is rare in corn-growing areas nationwide.
Copper, Ni, Co, Ti and V. The Emeishan LIP is generally considered to be the product of a mantle-plume event [22, 23] and characterized by high Cu, Ni, Co, Cr, Ti and V contents. In the southwestern part of the study region, areas with high Cu, Ni, Co, Cr, Ti and V contents in the top and deep soils overlap with the Emeishan basalt area, and the same holds true for the carbonate area in the southeastern part of the study region. This indicates that the spatial distributions of Cu, Ni, Co, Cr, Ti and V are mainly controlled by the Emeishan basalt and carbonate rock parent materials (Figs. 26-31). We showed in a statistical analysis that the average relative change rates of Cu, Ni, Co, Cr, Ti and V contents in the top soil, with respect to that in the deep soil (defined as (content in the top soil - content in the deep soil) / content in the deep soil) * 100) were -5.9 %, -5.31 %, -6.09 %, -6.52 %, -4.8 % and -2.58 %, respectively, demonstrating that the concentrations of these elements were all slightly lower in the top soil. In a correlation analysis comparing elevation with elemental content, we showed that the rates of Co and Ni loss in the top soil increased with increasing elevation (Fig. 32, a,b). The average rates of change of Cu, Cr, Ti and V contents in the top soil at different
Геоэкология Geoecology
Fig. 20. Lead distribution pattern in the top (0-20 cm) (a) and deep (150-180 cm) (b) soils of the Zhaotong - Bijie - Yibin - Luzhou - Leshan area Рис. 20. Схема распределения Pb в верхних (0-20 cm) (a) и глубоких (150-180 cm) (b) почвах в районе Чжаотун - Бицзе - Ибинь - Лучжоу - Лэшань
Геоэкология
Fig. 21. Zinc distribution pattern in the top (0-20 cm) (a) and deep (150-180 cm) (b) soils of the Zhaotong - Bijie - Yibin - Luzhou - Leshan area Рис. 21. Схема распределения Zn в верхних (0-20 cm) (a) и глубоких (150-180 cm) (b) почвах в районе Чжаотун - Бицзе - Ибинь - Лучжоу - Лэшань
Геоэкология
Cheng Hangxin, Peng Min, Zhao Chuandong, et al. Epigenetic geochemical dynamics.
Fig. 22. Silver distribution pattern in the top (0-20 cm) (a) and deep (150-180 cm) (b) soils of the Zhaotong - Bijie - Yibin - Luzhou - Leshan area Рис. 22. Схема распределения Ag в верхних (0-20 cm) (a) и глубоких (150-180 cm) (b) почвах в районе Чжаотун - Бицзе - Ибинь - Лучжоу - Лэшань
Геоэкология
Fig. 23. Cadmium distribution pattern in the top (0-20 cm) (a) and deep (150-180 cm) (b) soil of the Zhaotong - Bijie - Yibin - Luzhou - Leshan area Рис. 23. Схема распределения Cd в верхних (0-20 cm) (a) и глубоких (150-180 cm) (b) почвах в районе Чжаотун - Бицзе - Ибинь - Лучжоу - Лэшань
Геоэкология
Cheng Hangxin, Peng Min, Zhao Chuandong, et al. Epigenetic geochemical dynamics.
elevations were relatively consistent (Fig. 32, these five elements is essentially controlled by c-f), indicating the change of top soil contents of the same factors throughout the region.
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Fig. 24. Plot of Pb (a), Zn (b), Cd (c) and Ag (d) contents in the top and deep soils vs. elevation in the Zhaotong - Bijie - Yibin - Luzhou - Leshan area Рис. 24. График содержания Pb (a), Zn (b), Cd (c) и Ag (d) в верхних и глубоких почвах в зависимости от глубины в районе Чжаотун - Бицзе - Ибинь - Лучжоу - Лэшань
Table 3. Partial correlation analysis of Pb, Zn, Ag and Cd
with respect to Corg and pH in soils of the Zhaotong - Bijie - Yibin - Leshan - Luzhou area Таблица 3. Частичный корреляционный анализ содержаний Pb, Zn, Ag и Cd в соответствии с содержанием Corg и pH в почвах района Чжаотун - Бицзе - Ибинь - Лучжоу - Лэшань
Element Test parameters pH (constant Corg) Corg (constant pH)
Ag Correlation 0.055 0.817
Significance (two-tailed) 0.784 0
df 25 25
Cd Correlation -0.593 -0.323
Significance (two-tailed) 0.001 0.101
df 25 25
Pb Correlation -0.08 0.655
Significance (two-tailed) 0.692 0
df 25 25
Zn Correlation -0.583 -0.257
Significance (two-tailed) 0.001 0.195
df 25 25
Геоэкология
Fig. 25. Geochemical map of the Weining - Hezhang area, showing the locations of Zn smelting slag (adapted from [19]) and Cd (a) and Pb (b) contents in the top soils Рис. 25. Геохимическая карта района Вейнинг - Хечжан с указанием местонахождения цинкового шлака (по данным источника [19]), Cd (a) и Pb (b), содержащихся в верхних почвах
The analysis of driving factors of elemental content (Table 4) demonstrated that, the partial correlation coefficients of Cu, Ni, Co, Cr, Ti and V with respect to pH, were greater than those to organic carbon. This suggests that the loss of these elements in epigenetic environments is mainly driven by pH.
Conclusions and implications
Our study on driving mechanisms of the macroscopic distribution of elements in the top and deep soils of the Zhaotong - Bijie - Yibin -Luzhou - Leshan region clearly showed the
following: the geological environment determines the natural concentrations of chemical elements in soil; epigenetic geochemical processes reshape the microscopic distribution of elements in the top soil; biogeochemical processes drive the evolution of land quality; intensive human activities (such as mining) have disruptive impact on the natural evolution of elemental distribution. A better understanding of the dynamic geochemical processes on the Earth's surface can help to develop a theoretical framework, within which we can study the regional ecology formed through the interactions of topography, hydrology
Геоэкология
Fig. 26. Copper distribution pattern in the top (0-20 cm) (a) and deep (150-180 cm) (b) soils of the Zhaotong - Bijie - Yibin - Luzhou - Leshan area Рис. 26. Схема распределения Cu в верхних (0-20 см) (a) и глубоких (150-180 см) (b) почвах в районе Чжаотун - Бицзе - Ибинь - Лучжоу - Лэшань
Геоэкология
Fig. 27. Nickel distribution pattern in the top (0-20 cm) (a) and deep (150-180 cm) (b) soils of the Zhaotong - Bijie - Yibin - Luzhou - Leshan area Рис. 27. Схема распределения Ni в верхних (0-20 см) (a) и глубоких (150-180 см) (b) почвах в районе Чжаотун - Бицзе - Ибинь - Лучжоу - Лэшань
Геоэкология
Fig. 28. Cobalt distribution pattern in the top (0-20 cm) (a) and deep (150-180 cm) (b) soils of the Zhaotong - Bijie - Yibin - Luzhou - Leshan area Рис. 28. Схема распределения Co в верхних (0-20 см) (a) и глубоких (150-180 см) (b) почвах в районе Чжаотун - Бицзе - Ибинь - Лучжоу - Лэшань
Геоэкология
Fig. 29. Chromium distribution pattern in the top (0-20 cm) (a) and deep (150-180 cm) (b) soils
of the Zhaotong - Bijie - Yibin - Luzhou - Leshan area Рис. 29. Схема распределения Cr в верхних (0-20 см) (a) и глубоких (150-180 см) (b) почвах в районе Чжаотун - Бицзе - Ибинь - Лучжоу - Лэшань
Геоэкология
Cheng Hangxin, Peng Min, Zhao Chuandong, et al. Epigenetic geochemical dynamics.
Fig. 30. Titanium distribution pattern in the top (0-20 cm) (a) and deep (150-180 cm) (b) soils of the Zhaotong - Bijie - Yibin - Luzhou - Leshan area Рис. 30. Схема распределения Ti в верхних (0-20 см) (a) и глубоких (150-180 см) (b) почвах в районе Чжаотун - Бицзе - Ибинь - Лучжоу - Лэшань
Геоэкология
Fig. 31. Vanadium distribution pattern in the top (0-20 cm) (a) and deep (150-180 cm) (b) soils
of the Zhaotong - Bijie - Yibin - Luzhou - Leshan area Рис. 31. Схема распределения V в верхних (0-20 см) (a) и глубоких (150-180 см) (b) почвах в районе Чжаотун - Бицзе - Ибинь - Лучжоу - Лэшань
Геоэкология
Fig. 32. Relative change rate (Ri ) of Co (a), Ni (b), Cu (c), Cr (d), V (e) and Ti (f) contents in the top soil compared to that in the deep soil at different elevations in the Zhaotong - Bijie - Yibin - Luzhou - Leshan area
Ri = ((content in the top soil - content in the deep soil) / content in the deep soil) x 100) Рис. 32. Относительная скорость изменения (Ri ) содержания Co (a), Ni (b), Cu (c), Cr (d), V (e) и Ti (f) в верхних почвах по сравнению с глубокими почвами на разных высотах в районе Чжаотун - Бицзе - Ибинь - Лучжоу - Лэшань
Ri = ((содержание элемента в верхних почвах - содержание элемента в глубоких почвах / содержание элемента в глубоких почвах) х 100)
and land cover. Such framework has the potential for comprehensively integrating different scientific theories of Earth's systems. To study the physical, chemical and biodynamic processes on the Earth's surface, a new comprehensive survey and monitoring system for mountains, water bodies, forests, farmlands and grasslands is required. This system could help us determine the current natural resource usage, land quality, ecological quality and natural evolution patterns, and
assess land quality and future trends, so as to provide guidance for spatial planning and management nationwide.
China is a vast country with complex and diverse geographical landscapes [24]. In this study, we only analyzed the southwestern area characterized by mountains and gorges, and primarily revealed the mechanisms driving the macroscopic distribution of elements in the regional soils. Similar studies should be conducted in
Геоэкология
Table 4. Results of partial correlation analysis of Cu, Ni, Co, Ti and V
with respect to pH and Corg in soil in the Zhaotong - Bijie - Yibin - Luzhou - Leshan area
Таблица 4. Результаты частичного корреляционного анализа Cu, Ni, Co, Ti и V
по отношению к pH и Corg в почвах в районе Чжаотун - Бицзе - Ибинь - Лучжоу - Лэшань
Element Test parameter pH (constant Corg) Corg (constant pH)
Cu Correlation -0.841 0.407
Significance (two-tailed) 0 0.035
df 25 25
Ni Correlation -0.588 -0.337
Significance (two-tailed) 0.001 0.086
df 25 25
Co Correlation -0.741 -0.504
Significance (two-tailed) 0 0.007
df 25 25
Cr Correlation -0.58 -0.303
Significance (two-tailed) 0.002 0.124
df 25 25
Ti Correlation -0.847 0.403
Significance (two-tailed) 0 0.037
df 25 25
V Correlation -0.769 0.272
Significance (two-tailed) 0 0.169
df 25 25
future to analyze a variety of landscapes, including forests and swampy landscapes, humid and semi-humid low mountains, semi-arid hilly landscapes, alpine lakes in hilly landscapes, arid and semi-arid or humid and semi-humid alpine mountains, arid Gobi relict mountains, karst areas, alluvial plains, and colluvial deposits in the Gobi desert. Such studies would represent considerable advances in epigenetic geochemical dynamics and help us to establish a solid foundation for the development of scientific theories of the Earth's systems [25, 26].
Currently, surveys on the quantity, quality and ecological status of various natural resources in China are disconnected rather than combined in a single system. Presently, the Ministry of Natural Resources is responsible for all natural resource assets. It formulates land use regulations and
conducts ecological protection and restoration. However, a comprehensive survey and monitoring system, integrating the quantity, quality and ecological conditions of all natural resources based on their various transport patterns, remains to be developed. Moreover, chemical elements are the basic components of natural resources. For example, our findings on the epige-netic geochemical dynamic processes and mutual interactions of resources components, in the southwestern mountain and gorge regions, suggest that changes in chemical elemental contents in the environment are extremely sensitive indicators of environmental changes. Hence, we recommend that the chemical compositions of natural resources should also be included in the procedures during the development of future survey and monitoring systems.
References
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Геоэкология
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14. Hu Y, Li C, Wen H, et al. Characteristics of silver minerals in the lead-zinc-silver deposits at the junction of Sichuan, Yunnan, and Guizhou. Bulletin of Mineralogy, Petrology and Geochemistry. 2000;19(4):318-320.
15. Fuge R, Johnson C. The geochemistry of iodine: a review. Environmental Geochemistry and Health. 1986;8(2):31-54. https://doi.org/10.1007/BF02311063
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18. Fuge R. Soils and Iodine Deficiency. In: Selinus O (eds.). Essentials of medical geology: impacts of the natural environment on public health. Dordrecht: Springer Netherlands; 2013. p.417-432.
19. Peng Y. Study on the distribution and migration of heavy metals in slag, soil and plants in the indigenous zinc smelting district of Northwest Guizhou. Guiyang: Guizhou University; 2018.
20. Li Z, Feng X, Bi X, et al. Pollution status of heavy metals in soil on an indigenous zinc smelting site in Guizhou Province. Chinese Journal of Ecology. 2011 ;30(5):55—59.
21. Chen F, Dong Z, Wang C, et al. Pollution status and risk assessment of heavy metals in cultivated soil and crops in zinc smelting area. Environmental Science. 2017;38(10):376—385.
22. Li J, Zhong H, Zhu WG, Bai ZJ, Hu W. Elemental and Sr-Nd isotopic geochemistry of Permian Emeishan flood basalts in Zhaotong, Yunnan Province, SW China. International Journal of Earth Science. 2017;106(2):617-630. https://doi.org/10.1007/s00531-016-1326-z
23. Chung SL, Jahn BM. Plume-lithosphere interaction in generation of the Emeishan flood basalts at the Permian-Triassic boundary. Geology. 1995;23(10):889-892. https://doi.org/10.1130/0091-7613(1995)023<0889:PLIIG0> 2.3.CO;2
24. Xie X, Ren T. National geochemical mapping and environmental geochemistry - progress in China. Journal of Geochemical Exploration. 1993;49(1-2):15-34. https://doi.org/10.1016/0375-6742(93)90037-M
25. Lawton J. Earth system science. Science. 2001 ;292(5524):1965. https://doi.org/10.1126/science. 292.5524.1965
26. Bockheim JG, Gennadiyev AN. Soil-factorial models and earth-system science: a review. Geoderma. 2010;159(3-4):243-251.
Библиографический список
1. Hou Z. Support unified management and system restoration of natural resources based on earth system science // China Natural Resources News. 12.06.2018.
2. Li K., Peng M., Zhao C., et al. Twenty years of geochemical survey of national land quality // Earth Science Frontiers. 2019. Vol. 26. Iss. 5. P. 1-37.
3. Yang X., Wang P., Gao D. Climate change characteristics of Wumengshan National Nature Reserve from 1971 to 2015 // Journal of Northeast Forestry University. 2019. Vol. 47. Iss. 9. P. 71-75.
4. Ji Z., Huang Z., Xie G. Dry and wet climate changes in Yunnan from 1961 to 2010 // Meteorological Science and Technology. 2013. Vol. 41. Iss. 6. P. 1073-1079.
5. Xiao K., Xing S., Ding J., et al. Division of key mineralization zones of important solid minerals and
characteristics of resource potential in China // Acta Geologica Sinica. 2016. Vol. 90. Iss. 7. P. 1269-1280.
6. He L., Wu D., Zhao F., et al. Geological characteristics and ore prospecting model and ore prospecting direction of Hezhang Zhugongtang ultra-large lead-zinc deposit // Guizhou Geology. 2019. Vol. 36. Iss. 2. P. 106-109.
7. Xu Y., Zhong Y., Wei X., Chen J., Liu H., Xie W., et al. Evolution of Permian mantle plumes and surface systems // Bulletin of Mineralogy, Petrology and Geochemistry. 2017. Vol. 36. Iss. 3. P. 359-373.
8. Lin J. Spatiotemporal distribution and geological characteristics of the Permian basalt in the three provinces of Southwest China // Chinese Science Bulletin. 1985. Vol. 30. Iss. 12. P. 929-932.
Геоэкология
9. Ye J., Yao L. Discussions on the quality control method of regional geochemical survey sample analysis. Rock and Mineral Analysis. 2004;23(2):137-142.
10. Wang S., Ji H., Ouyang Z., et al. Preliminary study on the weathering of carbonate rocks // Science in China. Series D. 1999. Vol. 29. Iss. 5. P. 441-449.
11. Zhu L., Li J. Weathering of carbonate rocks and its environmental effects. Beijing: Geological Publishing House, 2004. 131 p.
12. Darnley A.G., Björklund A., B0lviken B., Gustavsson N., Koval P.V., Plant J.A., et al. A global geochemical database for environmental and resource management. Paris: UNESCO Publishing, 1995. 122 p.
13. Cui Z., Zhang H., Chen X., Zhang C., Ma W., Huang C., et al. Pursuing sustainable productivity with millions of smallholder farmers // Nature. 2018. Vol. 555. Iss. 7696. P. 363-366. https://doi.org/10.1038/nature25785
14. Hu Y., Li C., Wen H., et al. Characteristics of silver minerals in the lead-zinc-silver deposits at the junction of Sichuan, Yunnan, and Guizhou // Bulletin of Mineralogy, Petrology and Geochemistry. 2000. Vol. 19. Iss. 4. P. 318-320.
15. Fuge R., Johnson C. The geochemistry of iodine: a review // Environmental Geochemistry and Health. 1986. Vol. 8. Iss. 2. P. 31-54. https://doi.org/10.1007/BF02311063
16. Muramatsu Y., Yoshida S., Fehn U., Amachi S., Ohmomo Y. Studies with natural and anthropogenic iodine isotopes: iodine distribution and cycling in the global environment // Journal of Environmental Radioactivity. 2004. Vol. 74. Iss. 1-3. P. 221-232. https://doi.org/10.1016/ J.JENVRAD.2004.01.011
17. Yamaguchi N., Nakano M., Takamatsu R., Tanida H. Inorganic iodine incorporation into soil organic matter: evidence from iodine K-edge X-ray absorption near-edge structure // Journal of Environmental Radioactivity. 2010. Vol. 101. Iss. 6. P. 451-457. https://doi.org/10.1016/ j.jenvrad.2008.06.003
18. Fuge R. Soils and Iodine Deficiency // Essentials of medical geology: impacts of the natural environment on public health / eds. O. Selinus. Dordrecht: Springer Netherlands, 2013. P. 417-432.
19. Peng Y. Study on the distribution and migration of heavy metals in slag, soil and plants in the indigenous zinc smelting district of Northwest Guizhou. Guiyang: Guizhou University, 2018.
20. Li Z., Feng X., Bi X., et al. Pollution status of heavy metals in soil on an indigenous zinc smelting site in Guizhou Province // Chinese Journal of Ecology. 2011. Vol. 30. Iss. 5. P. 55-59.
21. Chen F., Dong Z., Wang C., et al. Pollution status and risk assessment of heavy metals in cultivated soil and crops in zinc smelting area // Environmental Science. 2017. Vol. 38. Iss. 10. P. 376-385.
22. Li J., Zhong H., Zhu W.G., Bai Z.J., Hu W. Elemental and Sr-Nd isotopic geochemistry of Permian Emeishan flood basalts in Zhaotong, Yunnan Province, SW China // International Journal of Earth Science. 2017. Vol. 106. Iss. 2. P. 617-630. https://doi.org/10.1007/s00531-016-1326-z
23. Chung S.L., Jahn B.M. Plume-lithosphere interaction in generation of the Emeishan flood basalts at the Permian-Triassic boundary // Geology. 1995. Vol. 23. Iss. 10. P. 889-892. https://doi.org/10.1130/0091-7613(1995)023<0889:PLIIGO>2.3.CO;2
24. Xie X., Ren T. National geochemical mapping and environmental geochemistry - progress in China // Journal of Geochemical Exploration. 1993. Vol. 49. Iss. 1-2. P. 15-34. https://doi.org/10.1016/0375-6742(93)90037-M
25. Lawton J. Earth system science // Science. 2001. Vol. 292. Iss. 5524. P. 1965. https://doi.org/10.1126/science.292.5524.1965
26. Bockheim J.G., Gennadiyev A.N. Soil-factorial models and earth-system science: a review // Geoderma. 2010. Vol. 159. Iss. 3-4. P. 243-251. https://doi.org/10.1016/j.geoderma.2010.09.005
Authorship criteria / Критерии авторства
Hangxin Cheng, Min Peng, Chuandong Zhao, Wei Han, Huiyan Wang, Qiaolin Wang, Fan Yang, Fugui Zhang, Chengwen Wang, Fei Liu, Yalong Zhou, Shiqi Tang, Kuo Li, Ke Yang, Zheng Yang, Xiaomeng Cheng, Ziwan Chen, Hua Zhang, Chunhu Mo are the authors of the article, hold equal copyright and bear equal responsibility for plagiarism.
Чэн Хансинь, Пэн Минь, Чжао Чуаньдун, Хань Вэй, Ван Хуйянь, Ван Цяолинь, Ян Фань, Чжан Фугуй, Ван Чэнвэнь, Лю Фэй, Чжоу Ялун, Тан Шици, Ли Ко, Ян Кэ, Ян Чжэн, Чэн Сяомэн, Чэнь Цзывань, Чжан Хуа, Мо Чуньху написали статью, имеют равные авторские права и несут одинаковую ответственность за плагиат.
Responsibility for plagiarism / Конфликт интересов
The authors declare that there is no conflict of interest regarding the publication of this article.
Авторы заявляют об отсутствии конфликта интересов.
All authors have read and approved the final version of this manuscript.
Все авторы прочитали и одобрили окончательный вариант рукописи.
Геоэкология
Information about the authors / Сведения об авторах
Hangxin Cheng,
Doctor's Degree, Professor,
Institute of Geophysical & Geochemical Exploration,
Chinese Academy of Geological Sciences,
84 Jinguang Road, Langfang 065000, China,
S] e-mail: [email protected]
Чэн Хансинь,
доктор,
профессор,
Институт геофизических и геохимических исследований Китайской академии геологических наук, 065000, г. Ланфан, ул. Цзиньгуан Роуд, 84, Китай, IS] e-mail: [email protected]
Min Peng,
Master's Degree, Engineer,
Institute of Geophysical & Geochemical Exploration,
Chinese Academy of Geological Sciences,
84 Jinguang Road, Langfang 065000, China,
School of Geosciences and Resources,
China University of Geosciences (Beijing),
29 Xueyuan Road, Beijing 100083, China,
e-mail: [email protected]
Пэн Минь,
магистр,
инженер,
Институт геофизических и геохимических исследований Китайской академии геологических наук, 065000, г. Ланфан, ул. Цзиньгуан Роуд, 84, Китай, Школа геологических наук и природных ресурсов, Китайский геологический университет (Пекин), 100083, г. Пекин, ул. Сюеюань Роуд, 29, Китай, e-mail: [email protected]
Chuandong Zhao,
Doctor's Degree, Professor,
Institute of Geophysical & Geochemical Exploration,
Chinese Academy of Geological Sciences,
84 Jinguang Road, Langfang 065000, China,
e-mail: [email protected]
Чжао Чуаньдун,
доктор,
профессор,
Институт геофизических и геохимических исследований Китайской академии геологических наук, 065000, г. Ланфан, ул. Цзиньгуан Роуд, 84, Китай, e-mail: [email protected]
Wei Han,
Master's Degree, Engineer,
Institute of Geophysical & Geochemical Exploration, Chinese Academy of Geological Sciences, 84 Jinguang Road, Langfang 065000, China, e-mail: [email protected]
Геоэкология
Хань Вэй,
магистр, инженер,
Институт геофизических и геохимических исследований Китайской академии геологических наук, 065000, г. Ланфан, ул. Цзиньгуан Роуд, 84, Китай, e-mail: [email protected]
Huiyan Wang,
Master's Degree, Engineer,
Institute of Geophysical & Geochemical Exploration, Chinese Academy of Geological Sciences,
84 Jinguang Road, Langfang 065000, China,
e-mail: [email protected]
Ван Хуйянь,
магистр,
инженер,
Институт геофизических и геохимических исследований Китайской академии геологических наук, 065000, г. Ланфан, ул. Цзиньгуан Роуд, 84, Китай, e-mail: [email protected]
Qiaolin Wang,
Master's Degree, Engineer,
Institute of Geophysical & Geochemical Exploration, Chinese Academy of Geological Sciences,
84 Jinguang Road, Langfang 065000, China,
e-mail: [email protected]
Ван Цяолинь,
магистр,
инженер,
Институт геофизических и геохимических исследований Китайской академии геологических наук, 065000, г. Ланфан, ул. Цзиньгуан Роуд, 84, Китай, e-mail: [email protected]
Fan Yang,
Doctor's Degree, Senior Engineer,
Institute of Geophysical & Geochemical Exploration, Chinese Academy of Geological Sciences,
84 Jinguang Road, Langfang 065000, China,
e-mail: [email protected]
Ян Фань,
доктор,
старший инженер,
Институт геофизических и геохимических исследований Китайской академии геологических наук, 065000, г. Ланфан, ул. Цзиньгуан Роуд, 84, Китай, e-mail: [email protected]
Fugui Zhang,
Master's Degree, Senior Engineer,
Institute of Geophysical & Geochemical Exploration, Chinese Academy of Geological Sciences,
84 Jinguang Road, Langfang 065000, China,
e-mail: [email protected]
Чжан Фугуй,
магистр,
старший инженер,
Институт геофизических и геохимических исследований Китайской академии геологических наук, 065000, г. Ланфан, ул. Цзиньгуан Роуд, 84, Китай, e-mail: [email protected]
Геоэкология
Chengwen Wang,
Master's Degree, Engineer,
Institute of Geophysical & Geochemical Exploration, Chinese Academy of Geological Sciences, 84 Jinguang Road, Langfang 065000, China, e-mail: [email protected] Ван Чэнвэнь,
магистр, инженер,
Институт геофизических и геохимических исследований Китайской академии геологических наук, 065000, г. Ланфан, ул. Цзиньгуан Роуд, 84, Китай, e-mail: [email protected]
Fei Liu,
Doctor's Degree, Senior Engineer,
Institute of Geophysical & Geochemical Exploration, Chinese Academy of Geological Sciences,
84 Jinguang Road, Langfang 065000, China,
e-mail: [email protected]
Лю Фэй,
доктор,
старший инженер,
Институт геофизических и геохимических исследований Китайской академии геологических наук, 065000, г. Ланфан, ул. Цзиньгуан Роуд, 84, Китай, e-mail: [email protected]
Yalong Zhou,
Master's Degree, Senior Engineer,
Institute of Geophysical & Geochemical Exploration, Chinese Academy of Geological Sciences,
84 Jinguang Road, Langfang 065000, China,
e-mail: [email protected]
Чжоу Ялун,
магистр,
старший инженер,
Институт геофизических и геохимических исследований Китайской академии геологических наук, 065000, г. Ланфан, ул. Цзиньгуан Роуд, 84, Китай, e-mail: [email protected]
Shiqi Tang,
Master's Degree, Assistant Engineer,
Institute of Geophysical & Geochemical Exploration, Chinese Academy of Geological Sciences,
84 Jinguang Road, Langfang 065000, China,
e-mail: [email protected]
Тан Шици,
магистр,
ассистент инженера,
Институт геофизических и геохимических исследований Китайской академии геологических наук, 065000, г. Ланфан, ул. Цзиньгуан Роуд, 84, Китай, e-mail: [email protected]
Kuo Li,
Master's Degree, Engineer,
Institute of Geophysical & Geochemical Exploration, Chinese Academy of Geological Sciences, 84 Jinguang Road, Langfang 065000, China, e-mail: [email protected]
Геоэкология
Ли Ко,
магистр, инженер,
Институт геофизических и геохимических исследований Китайской академии геологических наук, 065000, г. Ланфан, ул. Цзиньгуан Роуд, 84, Китай, e-mail: [email protected]
Ke Yang,
Doctor's Degree, Senior Engineer,
Institute of Geophysical & Geochemical Exploration, Chinese Academy of Geological Sciences,
84 Jinguang Road, Langfang 065000, China,
e-mail: [email protected]
Ян Кэ,
доктор,
старший инженер,
Институт геофизических и геохимических исследований Китайской академии геологических наук, 065000, г. Ланфан, ул. Цзиньгуан Роуд, 84, Китай, e-mail: [email protected]
Zheng Yang,
Master's Degree, Assistant Engineer,
Institute of Geophysical & Geochemical Exploration, Chinese Academy of Geological Sciences,
84 Jinguang Road, Langfang 065000, China,
e-mail: [email protected]
Ян Чжэн,
магистр,
ассистент инженера,
Институт геофизических и геохимических исследований Китайской академии геологических наук, 065000, г. Ланфан, ул. Цзиньгуан Роуд, 84, Китай, e-mail: [email protected]
Xiaomeng Cheng,
Master's Degree, Assistant Engineer,
Institute of Geophysical & Geochemical Exploration, Chinese Academy of Geological Sciences,
84 Jinguang Road, Langfang 065000, China,
e-mail: [email protected]
Чэн Сяомэн,
магистр,
ассистент инженера,
Институт геофизических и геохимических исследований Китайской академии геологических наук, 065000, г. Ланфан, ул. Цзиньгуан Роуд, 84, Китай, e-mail: [email protected]
Ziwan Chen,
Master's Degree, Senior Engineer,
Yunnan Institute of Geological Survey, 84 Renmin East Road, Kunming 650216, China, e-mail: [email protected] Чэнь Цзывань,
магистр,
старший инженер,
Юньнаньский институт Геологической службы, 650216, г. Куньмин, ул. Жэньминь Ист Роуд, 84, Китай, e-mail: [email protected]
Геоэкология
Hua Zhang,
Bachelor's Degree,
Senior Engineer,
Sichuan Geological Survey,
25 Renming Road, Chengdu 610081, China,
e-mail: [email protected]
Чжан Хуа,
бакалавр, старший инженер,
Сычуаньская геологическая служба,
610081, г. Чэнду, ул. Жэньминь Ист Роуд, 25, Китай,
e-mail: [email protected]
Chunhu Mo,
Bachelor's Degree,
Senior Engineer,
Guizhou Geological Survey,
171 Shilin West Road, Guiyang 550081, China,
e-mail: [email protected]
Мо Чуньху,
бакалавр,
старший инженер,
Геологическая служба Гуйчжоу,
550081, г. Гуйян, ул. Шилинь Вест Роуд, 171, Китай,
e-mail: [email protected]
Геоэкология
