In Mongolia there were two major glaciations in the early and late Pleistocene  , covering the Altai, Khangai, Khentii and Khuvsgul Mountain Ranges (Figure 1). There is evidence for three to four Pleistocene glaciations in the Altai overall, two to three Pleistocene glaciations in the Khangai and Khuvsgul, and one Pleistocene glaciation in the Khentii  . Today, glaciers occur in only a few mountains of the Altai, Khangai and Khuvsgul Mountain Ranges. The dominant style of glaciation recorded in the landforms and deposits of Mongolia is valley glaciation  including hanging glaciers along the mountain slopes and crests of highly-elevation mountains   . Modern glaciers in the high mountain ranges in Mongolia play a vital role in water resources in Central Asia, and also in regional ecological, social and economic development. Modern glaciers in the high mountain ranges provide over 70% of fresh water resources in Mongolia  and small mountain glaciers in high latitudes and high altitudes are very sensitive to climate change  . Thus climate change can modulate water resources through altering glacier mass balances  , and this has a large impact on regional development. There has been a lack of work linking glacier and surface water fluctuations, and the purpose of this paper is to provide such a connection for Mt. Ikh Turgen and Mt. Munkh Saridag in Mongolian Altai and Khuvsgul Mountain Ranges in western and northern Mongolia.
The Altai Mountain Range in Central Asia lies on the border between Mongolia, China, Kazakhstan and Russia (Figure 1). The Russian Altai has been the focus of much of the research to date on Altai paleoglaciation (e.g.  -  ), with additional work focused on the extents of Pleistocene and modern glaciers (including during the Little Ice Age) in the Mongolian Altai  -  . Several reviews summarize our knowledge of the extent of Pleistocene glaciations (e.g.       ), and previous work has suggested that the limited extent of past glacier expansion in the Mongolian Altai reflects decreasing precipitation and increasing ELAs from the northwest to the southeast of the Altai    . Although long-term fluctuations of glaciers over the Pleistocene in the Altai Mountain Range have been investigated in previous studies      , Holocene and modern glacier fluctuations in Mongolia have rarely been described   .
In the Khuvsgul Mountain Range, Tsegmid  estimated the extents of past glaciations based on glacial deposits, and absolute age dating suggests that maximum glacier advances were approximately synchronous across northern Mongolia  . Late Pleistocene glaciers around the Darkhad basin (Figure 2(B))
Figure 1. Location of the study areas in the Mongolian Altai and Khuvsgul Mountain Ranges. Red boxes with numbers denote locations in Figure 2.
Figure 2. Topography of the Mongolian Altai (A) and Khuvsgul (B) Mountain Ranges including study areas (red boxes), Mt. Ikh Turgen (A)and Mt. Munkh Saridag (B) in Figure 3 & Figure 4. These maps include locations of previous studies of paleoglaciology and glacial geomorphology.
advanced twice at 17 - 19 ka and 35 - 53 ka, when end moraines and ELAs were at ~1600 m a.s.l and 2100 - 2400 m a.s.l, respectively  in the surrounding Khuvsgul mountains (Figure 2(B)). The remnant end moraines and lateral moraines on the upper slopes and in the valleys of Rivers Tengis and Shishkhid, and intermontane basins (e.g.   ) indicate that large glaciers advanced in the Sayan and Khuvsgul Mountain Ranges in the late Pleistocene. During the latest extensive glaciations in the Late Pleistocene, Mt. Munkh Saridag was covered by ice from the Zhokhoiskiy and Okinskiy glaciers in the north, with an ice surface at 2100 - 2200 m a.s.l and an ice thickness of 300 - 400 m  . There was no glaciation during the Atlantic period (7000 - 7300 years ago) and modern glaciers have been present for the last 4000 - 5000 years  .
Today, modern glaciers and their landforms in the Mongolian Altai and Khuvsgul Mountain Ranges include ice caps, valley glaciers, hanging glaciers, cirques, hummocky terrain, moraines and moraine-dammed lakes. Modern glaciers remain only in the highest mountains of the Altai, and several studies have focused on estimating the total current glaciated area. Contemporary glacier coverage in the Mongolian Altai has been estimated using different methods and datasets as 328 km2  , >300 km2   , about 540 km2  , 659 km2   , around 850 km2  , 514 km2  , 423 km2  and 376.4 km2  . Additional studies of contemporary glaciation in the Mongolian Altai have provided detailed information for individual mountains and isolated massifs (e.g.    ). Glacier areas for Mt. Tsambagarav in the Mongolian Altai have been estimated at 74.8 km2  and 73.17 km2  . Lehmkuhl  calculated the extent of modern glaciers in the northeastern part of the Mongolian Altai to be 33.8 km2 for Mt. Turgen and 39.5 km2 for Mt. Kharkhiraa. Total glacier coverages for Mt. Ikh Turgen, Mt. Munkh Khairkhan and Mt. Sutai in the Mongolian Altai (Figure 2(A)) have been estimated to be 31.8 km2  , 26.58 km2 and 12.57 km2  , respectively. Recent studies show that modern glaciers occupy small areas in the mountain ranges of Mongolia, and that glaciated areas have been decreasing rapidly. Valley glaciers are sensitive indicators of regional and local climates  , and over a glacial cycle they respond to variations in the position and strength of major climate systems  . Current global climatic shifts are having a pronounced effect on glaciers in Mongolia  , however the extent of both paleo and modern glacier changes is still unclear. In terms of more recent glacier changes, Lehmkuhl  identified large-scale glacier retreat from Holocene and Little Ice Age limits to positions in 1948 and 1991 in the northeastern part of the Mongolian Altai, and Davaa  estimated a shrinkage of 22% in the size of glaciers in the Mongolian Altai Mountain Range as a whole during the last 50 - 60 years. This is a major concern in a region that depends so heavily on glacial meltwater to sustain water supplies for agriculture and other ecosystem services in summer months. The mean depth of Mongolian glaciers is 55.8 m and the total water resource accumulatedin the glaciers has been estimated at about 62.6 km3   . Over the last 40 years, the area under glaciers had decreased by 6%  . Although concerns about glacier loss and sustainable water supplies were among the reasons that monitoring stations for glacial studies in Mongolia were established on Mt. Tsambagarav in 2007, on Mt. Tavan Bogd in 2012 and on Mt. Turgen in 2013  , further work on the linkage between glaciology and hydrology in Mongolia is needed. Here, we consider the linkage between glacial and hydrological variations based on dynamic changes of modern glaciers in the Mongolian Altai and Khuvsgul Mountain Ranges in western and northern Mongolia, respectively (Figure 1), compared to climate and hydrological changes in these areas.
2. Study Area
2.1. Mongolian Altai Mountain Range
The Mongolian Altai Mountain Range (extending over 160,000 km2) is the most southeastern part of the Altai Mountain Range (over 248,900 km2) straddling the borders between Mongolia, China, Kazakhstan and Russia (Figure 1). The Mongolian Altai extends over 1000 km from Mt. Tavan Bogd (4374 m a.s.l) in the northwest to the Gichgene Mountain Range in the southeast  . In the Mongolian Altai, there are numerous branches and isolated mountains over 4000 m a.s.l. including Mt. Munkh Khairkhan (4231 m a.s.l.), Mt. Sutai (4226 m a.s.l.), Mt. Tsast Bogd (4208 m a.s.l.), Mt. Bugat (4041 m a.s.l.), Mt. Kharkhiraa (4040 m a.s.l), Mt. Ikh Turgen (4030 m a.s.l) and Mt. Turgen (4029 m a.s.l). Mt. Ikh Turgen, one of our study sites, is an isolated mountain in the southwest of Western Sayan Mountain Range on the border between Mongolia and Russia (Figure 1, Figure 2(A)).
Tectonically, the Mongolian Altai Mountain Range is an anticlinal ridge with intermontane valleys and depressions (Figure 2(A)) including the Depression of Great Lakes between the Mongolian Altai and Khangai Mountain Ranges, and the Valley of Lakes between the Govi Altai and Khangai Mountain Ranges. Geologically, the main mountains in the Mongolian Altai consist of dislocated Precambrian stratigraphic sequences and formations formed by mountain building movements during the late Tertiary and the early Quaternary  . The Mongolian and Govi Altai Mountain Ranges mainly consist of Archean and Proterozoic bedrocks. The Paleozoic deposits in the Altai-Sayan anticline belt were overlain by the Precambrian metamorphic rocks during the Caledonian mountain building movement  .
Morphogenetic features in the Mongolian Altai include the tectonic-denudational landforms, erosion-depositional landforms, and depositional landforms. Modern glaciers occupy areas of 85 km2 in the Potanin glaciers, 10 km2 at the head of River Sagsai, more than 20 km2 in Mt. Tsast Bogd, 66 km2 in Mt. Munkh Khairkhan, 21 km2 in Mt. Deluun, 25 km2 in Mt. Tsast, more than 60 km2 in Mt. Turgen, and 2 km2 in Mt. Tsengel Khairkhan (Figure 2(A)).
At the Ulgii and Khovd meteorological stations, annual average air temperature is 1.8˚C, and annual average precipitation is 56 mm in Ulgii and 210 mm in Khovd. The Mongolian Altai acts as a barrier for moisture travelling from the west and northwest in Russia to the east and southeast in Mongolia. Equilibrium Line Altitudes (ELAs) are at 3000 m a.s.l. and 3700 m a.s.l. in the northwestern and southeastern mountains of the Mongolian Altai, respectively  . Meltwater from glaciers in the Mongolian Altai feeds rivers, including the River Khovd, which is a source for Lakes Khoton, Khurgan and Khar Us in the Mongolian Altai (Figure 2(A)).
2.2. Khuvsgul Mountain Range
The Khuvsgul Mountain Range, the southeastern tip of the Eastern Sayan Mountain Range, is located in northern Mongolia (Figure 1). The Khuvsgul is surrounded by the Khangai Mountain Range in the south, isolated mountains in the drainage basins of Rivers Selenge and Orkhon in the southeast, and the Sayan Mountain Range in the north. The western mountains of the Khuvsgul are steep and sharply dissected by cliffs, whereas the northeastern and eastern mountains are gentle and domed-shaped. Most mountains in the Khuvsgul Mountain Range extend from southwest to northeast. Only Mt. Munkh Saridag, the highest peak in the Khuvsgul currently contains modern glaciers  . Bedrock in the Khuvsgul is largely schist, with granites in the Sayan Mountain Range and Mt. Ulaan Taiga, and carbonates in the Khoridol Saridag Mountain Range. Generally, carbonate and volcanic rocks underlie the western and the eastern Khuvsgul Mountains, respectively.
The predominant climate type in the Khuvsgul is an Eastern Siberian type of ultra-continental climate with a significant difference between winter and summer temperatures, high aridity, and large amplitudes of absolute maxima and minima  prevail. The annual average precipitation in the Khuvsgul is 190-300 mm at lower elevations and 400-500 mm in the high mountains. Most of precipitation is in July, evaporation is low, summers are cool, and winters are extremely cold. The annual average temperature amplitude is high due to cool summers. The annual average temperature is −1.9˚C with an annual air temperature amplitude of 70˚C - 80˚C and daily air temperature amplitude of 20˚C - 25˚C at the Khatgal meteorological station. These severe climatic conditions are responsible for the widespread existence of permafrost and associated cryogenic landforms in the Khuvsgul Mountain Range.
The Mt. Munkh Saridag (3491 m a.s.l) study site is the highest isolated mountain in the Khuvsgul Mountain Range and is located in the northeastern end of the Khuvsgul at the border between Mongolia and Russia (Figure 1, Figure 2(B)).
In this study, we reconstruct changes in glacier extent and connect this to previous observations of changes in both climate and hydrology. Changes in modern glaciers are estimated by comparing glacier extent from Landsat imagesfor Mt. Ikh Turgen (08/19/1998, 08/07/2002, 08/23/2011) and for Mt. Munkh Saridag (07/23/1986, 08/06/2000, 07/18/2007), 1:100,000 topographical maps (1970) and Google Earth. For satellite images with a high percentage of cloud cover, additional detail was provided using Google Earth’s 3D viewing capability. The extent of modern glaciers was mapped on the basis of ice limits identified visually from the remote sensing data and ASTER Global DEM data (AGDEM, 30 m resolution) (Figure 3, Figure 4). Snow indexes (NDSI) were calculated for Mt. Ikh Turgen and Mt. Munkh Saridag using a formula (NDSI = (GREEN − SWIR1)/(GREEN + SWIR1))  , to enhance the contrast between ice and snow. To predict potential future changes in glaciers, we used best-fit extrapolation
Figure 3. The extent and distribution of modern glaciers on Mt. Ikh Turgen (in blue) with background features of lowlands (in dark green) and mountains (in brown) on Landsat image, and features of past glaciation: 1) Glacial valley; 2) Glacial cirque and 3) Terminal moraine.
Figure 4. The extent and distribution of modern glaciers on Mt. Munkh Saridag (in blue) with background features of lowlands (in light green) and mountains (in pink) on Landsat image, and features of past glaciation: 1) Glacial valley; 2) Glacial cirque and 3) Terminal moraine.
of past changes to estimate the timescale over which glaciers are likely to disappear from each field area. Although simplistic, in the absence of more detailed data and models, this approach provides an estimate of the timescale of change that is helpful in conveying a sense of urgency about these changes to decision makers working on water resources management.
4. Results and Discussion
4.1. Modern Glaciers
Glacier mapping identifies ice caps, valley glaciers and hanging glaciers in the study areas (Figure 3, Figure 4). The area of modern glaciers on Mt. Ikh Turgen has decreased from 41.4 km2 in 1970, to 24.6 km2 in 1998, 21.69 km2 in 2002 and 18.9 km2 in 2011 (Figure 5). Thus glacier area has decreased by 45.6% between 1970 and 2011. The ELAs of the glaciers were at 2843 m and 3192 m a.s.l on the north and south aspects, respectively, in 1970, and increased to 2987 m and 3290 m a.s.l on the north and south aspects, respectively, by 2011, an increase in ELA elevation by 144 m and 98 m, respectively. The melt rate of the glaciers is higher on southeast, south and southwest facing aspects than on slopes with a northern aspect. A simple linear extrapolation of the empirical data suggests that the current glaciers remaining on Mt. Ikh Turgen will have melted away completely in ~27 years (Figure 5) if current climate changes continue. This is a general estimation and is intended to convey the approximate timescale of major change, rather then the exact year when the last ice will disappear.
On Mt. Munkh Saridag, modern glaciers remain as ice caps on top of the mountain plus in a few large cirques located at about 3000 m a.s.l. (Figure 2(B), Figure 4). Recent moraines associated with modern glaciers are located at 2705 ma.s.l. and there is a mass wasting surface 270 m wide and 500 m long adjacent to a small lake.Areas of modern glaciers on Mt. Munkh Saridag were 901 m2 in 1970, 850.1 m2 in 1986, 545 m2 in 2000 and 381 m2 in 2007. Thus the glaciated area has decreased by 57.3% between 1970 and 2007. Extrapolating the empirical data suggests that the current glaciers remaining on Mt. Munkh Saridag will have melted away completely in just a few years (Figure 6). This is a general estimate and is intended to convey the approximate timescale of major change, rather than the exact year when the last ice will disappear. During the period between 1970 and 2007 when the glacier extent was reduced by 57.3%, meteorological data indicate that there was a 2.16˚C increase in average annual temperature at the Khankh meteorological stations located 22 km from Mt. Munkh Saridag at an elevation of 1650 m a.s.l. In 1970, ELAs were at 2892 m and 3150 m a.s.l. on north and south aspects, respectively, and by 2007, these had risen to 2939 m and 3230 m a.s.l., representing an ELA elevation increases of 47 m and 80 m, respectively. The glaciers that occurred on southwest and west facing slopes in 1970 represented 4.1% of the ice area, and these had all disappeared completely by 2007. In 2007, 71.1% of total remaining glacier area was on north facing slopes. According to Kitov et al.  , a comparison with earlier data shows that the lower boundary of glaciers on Mt. Munkh Saridag was 2935 m a.s.l. in 2006, 2897 m a.s.l. in 1962, and 2803 m a.s.l. in 1906. Shrinkage of glaciers since
Figure 5. Recent glacier changes on Mt. Ikh Turgen (data on glacier area from this study). Linear extrapolation of this trend suggests that the glaciers will disappear by ~2042.
Figure 6. Recent glacier changes on Mt. Munkh Saridag (data on glacier area from this study). Non-linear extrapolation suggests that the glaciers will disappear by ~2017.
the end of the Little Ice Age has decreased glacier area by half (from 0.68 to 0.34 km2), over the past 160 years, glacier area on the Eastern Sayan Mountains decreased by 49%, and the terminus of the largest glacier retreated by 570 m in length and 124 m in height  . The work presented here allows for a comparison of modern changes in glacier extent for two mountains located at similar latitudes.
Although Mt. Munkh Saridag is located slightly further north (51˚40' - 51˚50'N latitude) than Mt. Ikh Turgen (49˚40' - 50˚00'N latitude), changes in modern glacier area on Mt. Munkh Saridag (57.3% reduction) are occurring slightly faster than on Mt. Ikh Turgen (45.6% reduction). The ELAs of the modern glaciers are rising faster on north and south aspects on Mt. Ikh Turgen than on Mt. Munkh Saridag. These differences may reflect the fact that the glacier extent on Mt. Munkh Saridag is much smaller than on Mt. Ikh Turgen. This difference in scale can also explain why the glacial lake area on Mt. Ikh Turgen has increased from 10.37 km2 in 1970 to 10.41 km2 in 2011 at the same time as the relatively large glaciers have been melting away, while glacial lake area on Mt. Munkh Saridag has decreased from 0.726 km2 in 1970 to 0.624 km2 in 2007 at the same time as the very small glaciers have shrunk in size. Extrapolating recent trends of glacier change suggest that Mt. Ikh Turgen and Mt. Munkh Saridag will be ice free in about 2042 and 2017, respectively (Figure 5, Figure 6).
Given the role that glaciers play in sustaining water flow during summer months, and the increase in annual flow that has come from recent glacier melt that has exceeded accumulation from snowfall, we predict that overall river flow, and in particular summer base flow in rivers fed by these glaciers, will decrease. Only if the loss of glacier melt is replaced by enhanced summer precipitation would river flow be maintained at current levels.
Overall, it is clear that modern glaciers in northern Mongolia vary significantly in size and have retreated at different rates depending on physical parameters such as topography, including elevation and aspect, vulnerability of the mountain glaciers to solar insolation, and duration of solar radiation for individual mountains. Previous studies   have documented rapid retreat of modern glaciers in Mongolia during periods of glacier observation (such as a ~29% reduction in glacier area in Mt. Tsambagarav between 1970 and 2000  ). Such changes are consistent with decreases in glacier areas in mountain ranges throughout the world that have been caused by global climate change   .
4.2. Surface Water
In this section we consider the linkage between glacial and hydrological fluctuations for Mt. Ikh Turgen and Mt. Munkh Saridag in western and northern Mongolia, respectively. Because Mongolia is very sensitive to climate change as a result of its geographic location and because of its socio-economic condition and reliance on pastoral animal husbandry, a nomadic way of life, and rain-fed agriculture, climate change that alters the Mongolian ecosystem and causes water shortages and desertification will result in severe economic impacts  . Hydrological changes driven by climate change and anthropogenic influences include enhanced glacier melt and permafrost thaw  . The maximum ice depth has decreased by 35 cm and the duration of ice cover has been shortened by 5 - 44 days  . The regime of spring floods has been advanced by 20 days in rivers draining the southern slopes of the Mongolian Altai and by 5 - 10 days in rivers draining the northern slopes of the Khuvsgul  . Average annual river flow in Mongolia (Figure 7) increased from the late 1970s to the early 1990s, and then decreased to 2010. However, during this later period of overall decrease, Davaa
Figure 7. Dynamics of the total river flow in Mongolia modified from Davaa (2010).
 observed that rivers draining the glaciated catchments of the Mongolian Altai Mountain Range and continuous permafrost catchments of the Khuvsgul Mountains increased in annual and seasonal flows  . The annual average water discharge of rivers draining from the Altai and Khuvsgul Mountain Ranges has increased by 15% - 35% in the last 30 - 70 years compared to long-term averages  . Similarly, lake area overall in Mongolia has decreased by 373 km2 in the last 60 years, with fluctuations including increases in area between 1960 and 1990 and further reductions since 1996, however lake areas have increased for large lakes located in the permafrost zone and lakes fed by glacier melt  . For example, since 1993 water levels in Lake Khuvsgul, located in the permafrost zone, have increased at the same time as water levels in Lakes Uvs and Khar Us, located in the arid zone have decreased  . Overall this suggests that during a period of overall reductions in surface water availability, ecosystems and human uses in catchments with permafrost and glaciers have been sustained by additional water from ice melt. However, the glacier component of this additional water will be lost as the glaciers disappear, likely leading to even more rapid hydrologic changes in the future than in other parts of Mongolia.
The average annual temperature in Mongolia has been increasing (Figure 8). Average annual temperature increased by 2.17˚C overall, and by 1.9˚C - 2.28˚C in the high mountains and 1.6˚C - 1.7˚C in the Govi desert since 1940  . Since 1940, the average winter temperature has been increasing noticeably as compared to the summer temperature, and winter precipitation increased while warm season precipitation decreased slightly  . These temperature increases and precipitation changes are likely to have driven observed changes in glacier extent, river discharge, and lake area. For the future, climate modeling based on the greenhouse gas (GHG) A1B scenario estimates an increase in average temperature in the next 100 years of 2.6˚C in winter and 2.4˚C in summer  . This temperature rise, coupled with changes to short, heavy rain instead of long-lasting rain events, will increase the stress on traditional herding lifestyles, thus affecting the social-ecological conditions of Mongolia  . It is predicted
Figure 8. Temperature trend between 1940 and 2001 in Mongolia, modified from Batima et al. (2005).
that decreases in snowfall, increased tree cutting, the melting of permafrost, intensifying drying trends, destruction of riparian zone shrubs and swamps, and overgrazing all interact, in a non-linear way, resulting in the disappearance of water sources including small streams, lakes and springs in central Mongolia as a result of the warmer and dryer climate  . A decline in the number of places to access surface water disrupts the traditional nomadic pastoral pattern of seasonal grazing. Similar trends of climate and ecological change have been identified in the Depression of Great Lakes region between Altai and Khangai Mountain Ranges. In this semi-arid region, surface water is a critical resource for both humans and animals.
In the early 21st century, when climate in Mongolia will continue to change dramatically  , global climate change, population growth, river damming, large-scale water abstractions, and rising levels of pollution exert multiple pressures on regional water resources  . Climate change response measures will help to address the inevitable need to adapt to meet the requirements of sustainable development strategies in Mongolia  .
4.3. Water Management
The ongoing rapid retreat and loss of glaciers in high mountains in Mongolia due to climate warming lead to challenges in the management of rivers and water resources. It is difficult to monitor the vast hydro-network in Mongolia, and to identify small lakes and disappearing glaciers, due to the fact that Mongolia occupies a large territory and has a low population density  . Thus hydrologic modeling based on climate change scenarios is an important basis for water management strategies. This type of modeling suggests that water stresses will increase under likely climate change scenarios  .
Mongolia has scarce water resources and will face major challenges to adapt to climate change, particularly in areas where enhanced water from glacier melt will be lost when the glaciers disappear. Global warming, and regional and local changes in water resources related to glacier melting and permafrost thawing will have a significant impact on environmental conditions, ecology, socio-economic outcomes, and human life. Management decisions that impact catchments are often made on the scale of political regions, rather than hydrologic regions (catchments)  . However management of a glacier-based catchment with numerous rivers and lakes basins that is likely to undergo major glacier melting-induced dynamical changes would be better approached in an integrated catchment-scale manner aimed at minimizing ecological and socio-economic impacts. For example, the catchments of the Altai and Khuvsgul Mountain Ranges should ideally be treated as transboundary regions covering four and two nations, respectively, with international coordination in management through Integrated River Basin Management (IRBM) that includes development of reservoirs to store glacier melting water for hydropower generation, drinking water, industrial and pasture water supply  . Protection of runoff formation zones is also needed, even if these are in different political regions than downstream areas, as is efficient and economic use of water resources and improved environmental monitoring (extension and modernization of the observation network), modeling, remote sensing, data integration and regional cooperation.
Mongolia has limited human, technical and financial capacities to solve the multi-faceted threat caused by climate change  , and because the impacts of climate change on the ecological system and natural resources in Mongolia will dramatically affect almost all sectors of the national economy, climate change response measures should address the need to adapt to climate change in ways that also archive the sustainable development strategies of Mongolia  . Numerous policies, plans and decisions for integrated environmental management have been made at national and international levels since joining the UN Framework Convention on Climate Change (UNFCCC) and the Kyoto Protocol in the 1990s. For example, the Parliament of Mongolia has passed several laws directed toward environmental protection, including the State Policy on Environment (1997), which forms the legal basis for the protection of Mongolia’s natural resources, and at the international level Mongolia has joined 14 environment-related UN Conventions and Treaties  . However, there is a gap between the plans and treaties and actual implementation on the ground, especially in remote areas.
In Central Asia, groundwater is shallow, rivers and lakes have unique water-dependent ecosystems, and human societies have developed in close integration with limited water resources  . It is in such situations that Integrated Water Resources Management (IWRM) has great potential to contribute to more secure livelihoods, increased environmental sustainability and greater social harmony. To archive this requires that water resources are managed efficiently, with minimization of unproductive water losses in water delivery and water demand  and proactive efforts to prepare for future changes in water availability. The Asia-Pacific Adaptation Network (APAN), a key regional initiative to build climate resilience of vulnerable human systems, ecosystems and economies through the mobilization of knowledge and technologies to support adaptation capacity building, policy-setting, planning, and best practices, can provide a road-map for good adaptation knowledge and practices in Mongolia. However, significant barriers persist for adaptation efforts in developing countries, including a lack of the necessary finance, knowledge, and technology for reducing vulnerability to climate change that is an important prerequisite for successful adaptation efforts  . Although IWRM requires a complete transdisciplinary assessment of the environmental and socio-economic conditions in local and regional contexts, studies such as that presented here contribute to the scientific base knowledge of changing precipitation-glacier-inflow-runoff-outflow-storage relationships that are necessary component of integrated decision making.
In the Mongolian Altai and the Khuvsgul Mountain Ranges in western and northern Mongolia, modern glaciers exist as small ice caps centered on the mountain peaks (Figure 3, Figure 4). The changing extent of these glaciers has significant impacts on water resources that must be considered in future water management.
Changes in modern glaciers have been dramatic since the 1970s. Glacier areas on Mt. Ikh Turgen in the Mongolian Altai and Mt. Munkh Saridag in the Khuvsgul Mountain Ranges have decreased by 45.6% between 1970 and 2011 and 57.3% between 1970 and 2007, respectively. Over the same period, the ELAs of the modern glaciers on Mt. Ikh Turgen have increased by 98 m and 144 m on north and south aspects, respectively, and on Mt. Munkh Saridag by 47 m and 80 m on north and south aspects, respectively. Although these mountains are located at similar latitudes, there is a faster reduction of glacier areas on Mt. Munkh Saridag and faster changes in ELA elevation on Mt. Ikh Turgen. These differences may reflect glacier scale and may also be related to differences in elevations and aspect, durations of solar radiation and vulnerability to the solar insolation for each individual mountain. Extrapolations of past change suggest that glaciers will be gone from Mt. Munkh Saridag in a few years, and from Mt. Ikh Turgen in a few decades. This will remove glacier melt as an important component of summer water supply for natural and human uses.
More sophisticated glaciological and hydrological observations and modeling is urgently needed to support local and regional water management policy and implementation. Integrated water management is the most suitable approach for this region, which includes diverse landscapes and ecosystems in catchments that cut across national and internal administrative units. Building on key linkages between glaciology and hydrology, future work should involve extensive fieldwork and modeling studies to examine the climate drivers that underlie modern glacier changes, as the basis for refined predictions of glaciological and hydrological changes that will be key to sustainable management of water resources in the changing Mongolian environment.
We would like to thank the Ministry of Environment and Green Development of Mongolia in Ulaanbaatar and its branch in Ulgii for their support to our field survey, and Dr. Robin Blomdin of Stockholm University for advice on remote sensing and mapping.