Anthropogenic Inﬂuences on Environmental Changes of Lake Bosten, the Largest Inland Freshwater Lake in China

: A short lacustrine sediment core (41 cm) from Lake Bosten in arid central Asia was used to investigate the environmental changes that occurred in the past ≈ 150 years based on the superposition of climate and anthropogenic factors. Geochemical elements, total organic carbon (TOC) and nitrogen (TN), and stable isotope data ( δ 13 C org and δ 15 N) were used to identify abnormal environmental changes. The average C / N ratio in the sediments of Lake Bosten suggested that the organic matter in lake sediments was mainly from aquatic plants. The δ 13 C org and δ 15 N in the lake sediments mainly reﬂect changes in the structure of the lake’s ecosystem. Before the 1960s, the primary productivity of the lake was relatively low with a relatively stable lake water environment. From the 1960s to the mid-1980s, the lake’s ecosystem was closely related to a signiﬁcant decline in water levels caused by human activities and an increase in salinity. From the late 1980s to ≈ 2000, the aquatic plant structure of Lake Bosten did not change signiﬁcantly. After 2000, the upper part of the sedimentary record suggested enhanced productivity due to urban and industrial development in the catchment area. However, sedimentary perspectives of the responses of di ﬀ erent environmental proxies in sediments to human activities were anisochronous, and the increasing heavy metal (Pb and Cu) and P accumulations appeared in 1970, reﬂecting heightened human impacts. Through the comparison between the Aral Sea and Lake Bosten, it was inferred that, under the intervention of human activities, the lake experienced a completely di ﬀ erent evolution trend. Humans, as geological agents, should protect our living environment while satisfying social development. The results will provide an important supplement to a large spatial scale study of the inﬂuences of human activities on the environment in Central Asia, which also has some signiﬁcant implications for the protection of the ecological environment and the realization of sustainable development in arid regions.


Introduction
As one of the most vulnerable terrestrial ecosystems, the arid regions of Central Asia are intertwined by the westerly circulation, the Arctic Ocean airflow, and the Indian Monsoon Current, making them sensitive to global change [1,2]. Humans, as geological agents [3,4], have profoundly changed the process of environmental evolution. Due to the combined effects of climate change and human activities, the regional land surface processes are undergoing extensive changes [5], which are illustrated by changes in the hydrological processes and the resulting ecological and environmental

Geographic Setting
The Lake Bosten watershed is located between the Tian Shan Mountains and the Taklamakan Desert ( Figure 1). The Lake Bosten watershed has an area of 45,000 km 2 and has a typical arid climate [45]. The total annual precipitation is only 76.1 mm, while evaporation is 2000 mm/year [26]. In the 1960s, 1174.86 km 2 of the watershed was covered by farmland; by the early 1990s, 760.41 km 2 of this area was covered by farmland [46]. There are six counties-Yanqi, Bohu, Hejing, Heshuo, Korla, and Yuli-in the Bosten watershed. Over the past 50 years, the economy has developed rapidly. The sums of several economic variables were calculated, including the year-end population, gross domestic product (GDP), total sown area for farm crops, and the number of industrial enterprises, to confirm the rapid growth in the region. For example, the GDP sharply increased from 5.6 × 10 6 Chinese Yuan (CNY, 1 USD = 6.9 CNY) in 1949 to 3.8 × 10 8   Bosten and the locations of sediment cores BTH01 and BST04H [45]. Lake Bosten was the largest freshwater body in north-western China and originates from the Kaidu River in the glaciated mountain ranges of Tian Shan; it is the source of the Peacock River (the source of Lop Nur) [47]. Lake Bosten is located at 1050 m above sea level and is 81 km long and 42 km wide, covering an surface area of 1005 km 2 [48]. Lake Bosten has undergone significant changes over Sustainability 2020, 12,711 4 of 14 the past fifty years. For example, the water level of Bosten Lake varies significantly with fluctuations of 5 m, and the salinity has increased from ≈0.4 g/L in 1958-1960 to 1.48 g/L in 2008 [48,49].
According to the distribution of aquatic plants in the lake [50], the most widely distributed species of aquatic plants are Ceratophyllum demersum, followed by Myriophyllum, Potamogetoncrispus, Potamogeton, and Najas marina. The submerged plant species are mainly present in the littoral zone (1-2 m water depth) and sub-littoral zone (5-6 m depth), while the deep-water areas have no submerged plants.

Sediment Sampling and Laboratory Analysis
In June 2016, a gravity core sediment sampler (Uwitec, Mondsee, Austria), fitted with a 60 mm internal diameter Perspex tube was used to extract a 41 cm long sediment core (41 • 55.665 N, 86 • 49.078 E) at a depth of 7.0 m in Lake Bosten (Figure 1c). According to the site description, the core consists of fine silt with a dark brown colour. Since no significant sedimentary events were found, the core was evenly sliced at 1 cm intervals in situ, and the samples were freeze-dried for laboratory analysis. All the analyses were conducted at the analytical centre of the State Key Laboratory of Lake Science and Environment, Nanjing, China.
A part of each sample of dried sediment was analyzed for 210 Pb, 226 Ra, and 137 Cs using an EG&G Ortec Gamma Spectrometer (HPGe GWL-120-15, EG&G/ORTEC, Tennessee, USA) [51]. The activity of 226 Ra in the lake sediments was evaluated by averaging the activities of 214 Pb (295 keV, 352 keV) and 214 Bi (609 keV). The total 210 Pb was determined via its emissions at 46.5 keV, and the total 137 Cs was determined via its emissions at 662 keV. The determination of total organic carbon (TOC) and total nitrogen (TN) were performed using a CE-440 elemental analyser (EAI Company, Lexington, KY, USA) [52]. The levels of δ 13 C and δ 15 N were analyzed using a Finnigan-MAT 251 isotope ratio mass spectrometer (Finnigan MAT, Bremen, Germany) [21]. These levels are expressed in standard per mil (% ) notation relative to the international standards, Vienna Pee Dee Belemnite and atmospheric N, respectively. The average reproducibility for δ 13 C and δ 15 N were 0.05% and 0.25% , respectively. Aluminium (Al), iron (Fe), and zinc (Zn) were analysed using a Leeman Labs Profile Inductively Coupled Plasma Spectrometer (ICP-AES, Prodigy, Teledyne Leeman Labs, Hudson NH, USA) and inductively coupled plasma mass spectrometry (ICP-MS, Agilent 7700x; Agilent Technologies, Santa Clara, USA) for copper (Cu) and lead (Pb). The correlation coefficient and its matrix were used to reflect the relationship between elements (Al, Fe, Zn, Cu, and Pb).

Data Collection for Instrumental Records
In order to study the differences of the impact of human activities on nature under the same climate change background, we compared the measured records of Bosten Lake and the Aral Sea. Dynamics of fish catches in the Aral Sea were taken from the reference [53]. Annual precipitation (mm) was recorded at the Yanqi weather station (location in Figure 1). Precipitation data within the Aral Sea drainage basin were referred to in reference [54]. The data for Lake Bosten water volume and river inflow to Lake Bosten were recorded in reference [55]. The data of Amu Darya inflows to the Aral Sea were from reference [56], and the water volume of the Aral Sea were recorded in reference [41].

The Chronology of the Bosten Lake Sediment Core
The specific activity of the excess 210 Pb was obtained by measuring the amount of 210 Pb and 226 Ra within a layer [57]. 210 Pb and 226 Ra were in equilibrium at 39 cm, and the chronology of the Lake Bosten sediment was established using the constant rate of supply (CRS) model [58] supported by 210 Pb ex data ( 210 Pb ex = 210 Pb − 226 Ra).
The characteristics of the specific activity of 137 Cs with depth in lake sediment cores are shown in a previously published paper [57]. There has been significant measurable global fallout of 137 Cs since 1954 [59], and this fallout marked the Lake Bosten sediment core at 29 cm, which is perfectly consistent with the 210 Pb dating. In general, there should be a global 137 Cs fallout peak at 1963; however, the Lake Bosten watershed is a unique nuclear test zone in China. The core sediments recorded the local bomb tests with a peak in 1976 [45], which is in good agreement with the date inferred from 210 Pb.

Organic Matter Proxies and Their Reponses to Anthropogenic Influences
The average TOC is 2.7%, with a maximum of 3.5% and a minimum of 2.1%. From the baseline to 1960, there is an increasing trend for organic carbon content. Then, there is a decrease until 1980 with a minimum value of 2.1%. Since 1980, the organic carbon content gradually increases again. The average TN of the sediments is 0.53%, with a maximum of 0.75% and a minimum of 0.40%. There are obvious similarities between TOC and TN ( Figure 2).
The specific activity of the excess 210 Pb was obtained by measuring the amount of 210 Pb and 226 Ra within a layer [57]. 210 Pb and 226 Ra were in equilibrium at 39 cm, and the chronology of the Lake Bosten sediment was established using the constant rate of supply (CRS) model [58] supported by 210 Pbex data ( 210 Pbex = 210 Pb − 226 Ra).
The characteristics of the specific activity of 137 Cs with depth in lake sediment cores are shown in a previously published paper [57]. There has been significant measurable global fallout of 137 Cs since 1954 [59], and this fallout marked the Lake Bosten sediment core at 29 cm, which is perfectly consistent with the 210 Pb dating. In general, there should be a global 137 Cs fallout peak at 1963; however, the Lake Bosten watershed is a unique nuclear test zone in China. The core sediments recorded the local bomb tests with a peak in 1976 [45], which is in good agreement with the date inferred from 210 Pb.

Organic Matter Proxies and Their Reponses to Anthropogenic Influences
The average TOC is 2.7%, with a maximum of 3.5% and a minimum of 2.1%. From the baseline to 1960, there is an increasing trend for organic carbon content. Then, there is a decrease until 1980 with a minimum value of 2.1%. Since 1980, the organic carbon content gradually increases again. The average TN of the sediments is 0.53%, with a maximum of 0.75% and a minimum of 0.40%. There are obvious similarities between TOC and TN ( Figure 2).  The organic materials, TOC, and TN in the lake sediments are mainly controlled by the initial productivity of the lake and by the input of terrigenous organic debris [60,61]. Different sources of organic matter have different C/N ratios-for example, the TOC/TN ratio. Aquatic phytoplankton are mainly rich in protein and organic nitrogen, so the C/N ratio is low (from four to 10). Terrestrial vascular plants are composed mainly of lignin and cellulose and lack nitrogen; thus, the C/N value of terrigenous organic matter is usually 20-30 [62]. The C/N ratio of lake sediments has been widely used to distinguish the source of sedimentary organic matter [63,64]. When the C/N ratio is less than 10, the organic matter is derived from aquatic plants; when the C/N ratio is greater than 20, the organic matter is derived from terrestrial plants. Therefore, the C/N ratio can be used to determine the source of the organic matter during the formation of sedimentary sequences. The average C/N ratio in the sediments of Lake Bosten is 6.1. The maximum value is 8.4, recorded ca. 1960. The results suggested the organic matter was mainly from aquatic plants and inferred the initial productivity in the lake. The variations in the organic geochemical proxies of the core sediments from Lake Bosten are shown in Figure 2. The average TOC is 2.7%, with a maximum of 3.5% and a minimum of 2.1%. From the baseline to 1960, there is an increasing trend for organic carbon content. Then, there is a significant decrease until 1980, with a minimum value of 2.1%. Since 1980, the organic carbon content gradually increases again. The average TN of the sediments is 0.53%, with a maximum of 0.75% and a minimum value of 0.40%. There are obvious similarities between TOC and TN.
The δ 13 C org values vary from −22.84% to −26.86% . From 1868 to 1960, the isotopic values show a slight increase. From 1960, the organic carbon isotopic values are negative, with an average value of −26.31% , which is contrary to the trend of nitrogen isotope δ 15 N. From 1960, the organic carbon isotopic values are negative, with an average value of −26.31% . The δ 13 C org values in lake sediments are mainly determined by the source of the organic matter in the lake sediments, which is generally influenced by a mixture of terrestrial plants, aquatic plants, and plankton [52]. In addition, the δ 13 C org content is affected by the lake chemistry (pH, water hardness, etc.), primary lake productivity, atmospheric carbon dioxide concentration, watershed hydrology characteristics, regional natural environment, sedimentary environment, and sedimentation [65]. Based on the C/N ratio, the organic matter in the sediments from Lake Bosten is mainly derived from lacustrine aquatic plants. Aquatic plants can be divided into floating plants and submerged plants based on the source of the CO 2 they use for photosynthesis. Floating plants include emergent plants, phytoplankton, and floating-leaf plants.
The δ 13 C values of floating plants are close to the δ 13 C values of terrestrial C 3 plants, usually ranging from −22% to −33% [66]. Photosynthesis and the growth of submerged plants are affected by the water bodies they grow in. Restrictions in the supply of dissolved CO 2 will cause the plants to use HCO 3 for their growth. Under normal temperature conditions, the value of δ 13 C in HCO 3 is greater than that of dissolved δ 13 C (CO 2 ) by 8.8% to 11.5% , resulting in positive δ 13 C values for submerged plants (−20% to −12% ) [66]. In addition, as the amount of photosynthesis continues to increase, more 12 C is selectively removed from the surface waters of the lake, which can result in the aquatic plants being enriched in 13 C, causing the δ 13 C content of the aquatic organic matter to increase.
From 1868 to 1960, the nitrogen isotope values are low. From 1960 to 1980, the nitrogen isotope values increase significantly. From 1980, the nitrogen isotope values are high, and the variations in organic carbon and nitrogen isotopic values have a significant correlation coefficient R 2 = 0.953 (p < 0.01). The soil nitrogen in the catchment was derived from atmospheric nitrogen fixed by nitrogen-fixing bacteria. The δ 15 N value of the soil is similar to the atmospheric nitrogen δ 15 N value (0% ), which was much smaller than the δ 15 N value of the dissolved inorganic nitrogen (DIN) in the lake water [66]. Therefore, if there is an increase in precipitation in the lake watershed, the lake water's DIN reservoir will be depleted in 15 [67].
The climate was cold and humid during the little ice age (LIA) (ca. 1500-1900) in this region [45]. From the end of the LIA to 1960, as the global climate warmed, the primary productivity of the lake increased. There was no significant sudden change in δ 13 C and δ 15 N levels during this period, indicating that the lake environment would have been relatively stable. However, there is a discontinuity at 1960 (Figure 2). Since 1960, the TOC, TN and δ 13 C levels significantly decreased, reflecting a significant decrease in the primary productivity of the lake. This decrease in productivity is closely related to the significant decline in water level and increased water salinity caused by enhanced water demands ( Figure 3). As the lake's water level decreased, sediment nitrification was enhanced (Figure 3).
increased. There was no significant sudden change in δ 13 C and δ 15 N levels during this period, indicating that the lake environment would have been relatively stable. However, there is a discontinuity at 1960 (Figure 2). Since 1960, the TOC, TN and δ 13 C levels significantly decreased, reflecting a significant decrease in the primary productivity of the lake. This decrease in productivity is closely related to the significant decline in water level and increased water salinity caused by enhanced water demands ( Figure 3). As the lake's water level decreased, sediment nitrification was enhanced ( Figure 3). annual precipitation (mm) recorded at the Yanqi weather station (location in Figure 1); (h) precipitation data within the Aral Sea drainage basin [54].(i) variations in inflow to Lake Bosten [55]; (j) Lake Bosten water volume (km 3 ); (k) Amu Darya inflows to the Aral Sea [56]; (l) percentage of the maximum volume for Aral Sea [41]. For the sake of timing comparison, all curves have the same ycoordinates.

Geochemical Elements and Their Reponses to Anthropogenic Influences
Elemental contents are shown in Figure 4. The maximum value of Al is 37.14 g kg −1 , and the minimum value is 27.03 g kg −1 . The concentration of Al was very similar to that of Fe (maximum is 19.05 g kg −1 and minimum is 14.13 g kg −1 ). The elements Pb, and Cu have a generally consistent trend. The maximum and minimum values of Pb were 13.75 mg kg −1 are 7.92 mg kg −1 , respectively. There is also same variation in trends among the Pb and Cu (maximum is 16.82 mg kg −1 and minimum is 11.58 mg kg −1 ).

Geochemical Elements and Their Reponses to Anthropogenic Influences
Elemental contents are shown in Figure 4. The maximum value of Al is 37.14 g kg −1 , and the minimum value is 27.03 g kg −1 . The concentration of Al was very similar to that of Fe (maximum is 19.05 g kg −1 and minimum is 14.13 g kg −1 ). The elements Pb, and Cu have a generally consistent trend. The maximum and minimum values of Pb were 13.75 mg kg −1 are 7.92 mg kg −1 , respectively. There is also same variation in trends among the Pb and Cu (maximum is 16.82 mg kg −1 and minimum is 11.58 mg kg −1 ).
Human activities have had an important influence on the source of terrigenous clastic materials in the lacustrine sediments of Lake Bosten. From the variation trend of the elements (Figure 4), the geochemical changes were obviously different before and after 1970. The vertical distributions of Pb and Cu mainly increased from 1970 until the present. In addition, the decrease of Pb content can be observed in the upper sediment layers (from ≈2005). At Stage A (since 1970), the potentially toxic elements (Pb and Cu) have negative correlations with Al and Fe ( Figure 5). At Stage B (from 1868 to 1970), there are significant correlations among all elements, which indicated the same material sources. Generally, Al [68] and Fe [69] are from terrigenous clastic material, which is mainly derived from erosion/catchment soils. This phenomenon suggested that Pb and Cu have been influenced by anthropogenic contributions. Some of the elements are not only or predominately derived from the catchment (i.e., erosion) but also from atmospheric deposition. Furthermore, the decrease in Pb contents in the upper sediment layers (from ≈2005) may show reduced atmospheric Pb pollution due to legal regulations. The studies of surface soils [70,71] and lake sediments [24] in arid regions of Central Asia show that heavy metals-such as Pb, Cu, and Zn-generally represent pollution by Human activities have had an important influence on the source of terrigenous clastic materials in the lacustrine sediments of Lake Bosten. From the variation trend of the elements (Figure 4), the geochemical changes were obviously different before and after 1970. The vertical distributions of Pb and Cu mainly increased from 1970 until the present. In addition, the decrease of Pb content can be observed in the upper sediment layers (from ≈2005). At Stage A (since 1970), the potentially toxic elements (Pb and Cu) have negative correlations with Al and Fe ( Figure 5). At Stage B (from 1868 to 1970), there are significant correlations among all elements, which indicated the same material sources. Generally, Al [68] and Fe [69] are from terrigenous clastic material, which is mainly derived from erosion/catchment soils. This phenomenon suggested that Pb and Cu have been influenced by anthropogenic contributions. Some of the elements are not only or predominately derived from the catchment (i.e., erosion) but also from atmospheric deposition. Furthermore, the decrease in Pb contents in the upper sediment layers (from ≈2005) may show reduced atmospheric Pb pollution due to legal regulations. The studies of surface soils [70,71] and lake sediments [24] in arid regions of Central Asia show that heavy metals-such as Pb, Cu, and Zn-generally represent pollution by human activities; however, Zn in the sediments of Lake Bosten has not shown signs of significant influence by human activities.

Regional Comparisions for Environmental Changes under Anthropogenic Influences in Central Asia
In this paper, sedimentary perspectives of the responses of different environmental proxies in sediments to human activities were anisochronous. There was no significant sudden change in δ 13 C

Regional Comparisions for Environmental Changes under Anthropogenic Influences in Central Asia
In this paper, sedimentary perspectives of the responses of different environmental proxies in sediments to human activities were anisochronous. There was no significant sudden change in δ 13 C and δ 15 N levels during this period, indicating that the lake environment would have been relatively stable. However, there is a discontinuity at 1960 (Figure 3). Since 1960, the TOC, TN, and δ 13 C levels significantly decreased, reflecting a significant decrease in the primary productivity of the lake. However, the study of the geochemical elements in sediments of Lake Bosten shows that the sedimentary sources had changed since the 1970s. Through the above discussion, it can be preliminarily concluded that sedimentological proxies are the perspectives of different environmental factors; however, the complexity of sedimentological responses allows a single proxy to imply the history of human activity and likely be limited by regional human conditions.
According to the existing studies on lake sediments in arid areas of Central Asia, the significant enhancement of human activities had led to significant changes in the sources of lake sediments. Among them, in the region of north Tianshan Mountains, important changes in sedimentary sources had taken place in the mid-1950s for Lake Ebinur (Figure 1) [22], for Lake Sayram (Figure 1) [23] in the 1960s, and for Lake Chaiwopu (Figure 1) in the 1950s [24], reflecting the temporal differences in the intensity of human activities in different regions. In terms of the changes in the impact of human activities on the lake ecosystem, although Ebinur Lake also experienced a significant contraction since the 1950s [44], which is consistent with the change of water level in Lake Bosten [72], the organic geochemistry proxies of Ebinur Lake, as a salt lake, maintained a certain stability [22]. However, the variation of organic carbon isotopes in the sediments of Lake Chaiwopu, a small shallow lake, is controlled by regional temperature [21]. In summary, due to the influence of different lake hydrological characteristics, the response of lake ecosystem to human activities and climate change shows great spatial variation.
According to instrumental records, the water level and water storage of Lake Bosten has declined since 2002, and the water salinity changed from falling to rising in 2004 [55] (Figure 3). The response of the lake ecosystem to different influencing factors is not consistent. In particular, the recent effect of the water salinity of Lake Bosten is much smaller than that of nutrient materials. In addition, the impact of human intervention on the lake ecosystem is also great. There are many similarities in the changes of the lake environments between the Aral Sea and Lake Bosten. By comparing the Aral Sea and Lake Bosten (Figure 3), it is found that the water storage of these two lakes continued to decline in the 1950s, and the water environment of both lakes was at its worst around the 1980s. In the 1980s, when the water salinity of the Aral Sea exceeded 18 g L/1, the Aral Sea had completely lost fishery [53], and there were only 1-5 fish species in the 1980s compared with 20 species in 1961 AD [73]. Tarim schizothoracin (Schizothorax biddulphi Günther) of Lake Bosten, which is only distributed in the Tarim Basin of the Xinjiang Autonomous Region in China [74], has also disappeared due to the high salinity of Lake Bosten (Figure 3) [49]. During this stage, the TOC and TN were both at minimum values in the sedimentary records of Lake Bosten, indicating that the lake's primary productivity was at its lowest value over the past 150 years.
To artificially intervene in the falling trend of lake water levels, the local government constructed a pumping station in the eastern part of Lake Bosten in 1983 to adjust the outflow to the Peacock River. Meanwhile, the decreased water consumption due to drip irrigation, mulching and other agricultural water-saving technologies, and enhanced watershed precipitation [55] has induced an increase in water levels since 1985 ( Figure 3). Although precipitation in the Aral Sea has also increased since the late 1980s [54], the inflow of water entering the lake is consistently low [56], which has been due to prominent contradictions in the allocation of water resources between Central Asian countries and a lack of centralised and effective water resources utilization policies. The Aral Sea separated into northern (Small Aral Sea) and southern (Big Aral Sea) bodies in 1987 [75]. An earthen dike was constructed in 1992 to block the Syr Darya River inflow to the Big Aral Sea [76], and in 1996-1997, a very large dam was constructed to raise the level of the Small Aral Sea [77], which was a successful experiment and demonstration of stabilizing lower salinity and improving ecological and fishery conditions in the Small Aral Sea [78]. However, the Big Aral Sea is on the verge of disappearing; according to projections, the eastern part of the Big Aral Sea will basically disappear by 2025 [79]. Through the comparison between the Aral Sea and Lake Bosten, it was inferred that, under the intervention of human activities, the lake experienced a completely different evolution trend. Humans, as geologic agents [3,4], should protect our living environment while satisfying social development.

Conclusions
The geochemical proxies in the lacustrine sediments of Lake Bosten in arid Central Asia provide an example of abnormal environmental changes under climate change and human activities over the past ≈150 years, providing will provide an important supplement to large spatial scale studies of the influences of human activities on the environment in Central Asia.
(1) In this paper, sedimentary perspectives of the responses of different environmental proxies in sediments to human activities were anisochronous, and the complexity of sedimentological responses allows a single proxy to imply the history of human activity and is likely to be limited by regional human conditions. (2) The average C/N ratio in the sediments of Lake Bosten suggested that the organic matter in lake sediments mainly comes from aquatic plants. The stable isotope δ 13 C org suggested changes in the composition of aquatic plants in lakes, which is closely related to the significant decline in the water levels and increased water salinity caused by enhanced water demands. The geochemical proxies of lake sediments did not respond to the changes since the late 1980s with increased water levels and improved water quality. (3) Human activities have had an important influence on the source of terrigenous clastic materials in the lacustrine sediments of Lake Bosten. The heavy metals (Cu and Pb) in Stage A, that is, from 1970, are not correlated positively with Al (which is mainly derived from erosion/catchment soils), reflecting enhanced human impacts. (4) According to the regional comparison, the period of significant enhancement of human activity recorded by the Bosten Lake sediment in the south of Tianshan is later than that in the north of Tianshan. (5) In areas with similar natural backgrounds, the evolution of lakes (Lake Bosten and theAral Sea) have completely different forms under the intervention of human activities, reflecting that the influence mode and intensity of human activities must be controlled. This also has significant implications for the protection of the ecological environment and the realization of sustainable development in arid regions.