Posted on Authorea 16 Dec 2019 | CC BY 4.0 | https://doi.org/10.22541/au.157652715.56884600 | This a preprint and has not been peer reviewed. Data may be preliminary. onanrvr,adteei vdneta h ubro xrm vnsaetn onanrvr has rivers mountain in affecting relevant events particularly is extreme issue 2016; of This and lowland (UNOCHA, number 2016). Nikiforova, both damages the and displacing affect (Kozhakhmetov country, in that years Floods the recent million evidence livestock. in in $30 and is caused 80% hazards by crops than there Floods natural increased infrastructure, more and severe of average 2016). most loss rivers, annual on through Nikiforova, the mountain 2018) of causing of and al., 75% one and (Kozhakhmetov et than are year spring Guha-Sapir more melt liquid each with early snow and from people runoff, in spring times 10-30,000 contributions annual and period 5-7 winter the in by short late variability runoff dwarfing a by large annual in use, average by represents occurring industrial exceeding snowmelt characterized runoff discharges climate Kazakhstan, and are by annual In rivers agricultural exacerbated an largest 2019). further Kazakh for provides the al., be groundwater; melt water et can or cover which Han of issue precipitation 2014; snow source an al., Snow climate, hazards, primary et populations. continental natural (Dietz the local of intervention and the source human arid for a and freshwater the as change of act to availability also the owing however, determining can, Asia, runoff, Central to contribution of important regions the In countries. easily other is and approach Kazakhstan Introduction Our in 1 strategies Irtysh. winter management the The flood for retreat. support forecasts cover snow could runoff upon spring and long-term in catchments, anomalies into pattern similar pressure incorporated circulation other scale atmospheric be to 500-2000 large this therefore elevations transferable of the at could winter effect of particularly with lagged index impact disappearance, a basin Oscillation cover the suggests largest snow Arctic This is of the driver timing level. for in resultant sea primary 0.82 and day-1 above The to temperatures km2 m up air 5900 region. of (MAM) exceeded 14 the spring correlations and over and mean significant period Oscillation the shows March the study Arctic spring contrast, 22 the the In in over between of disappearance trend period. occurs snow indices observation increasing retreat of the weak over disappearance timing cover a trend cover The displays snow clear snow the rate no 2017. peak and depletion evaluated but average, cover variations rate possible we inter-annual snow on a depletion study, large peak cover that as with annual this snow 2017 found basin, In and the We peak on 2000 of depending between area. dataset. time April basin the MOD10A2 the Irtysh in MODIS assessing Upper snow-induced events, the resources the these flood of water from of spring sub-basins of timing of major the management each five factor influence the floods in that explanatory spring cover for processes by snow scale critical affected winter-spring severely large but in is the variability lacking, basin of upper currently Knowledge its snowmelt. is and of Kazakhstan floods result eastern a of as resource water primarily main year, the is River Irtysh The Abstract 2020 5, May 4 3 2 1 Fugazza Davide Central basin, Irtysh Upper Asia the in and indices patterns circulation depletion atmospheric cover snow in variability Inter-annual nvriyo otubi tNewcastle at Northumbria of University University National Eurasian Gumilev Lev Center Technology Mining Advanced Milan of University 1 hmsShaw Thomas , 2 hmhglMashtayeva Shamshagul , 1 3 n e Brock Ben and , 4 Posted on Authorea 16 Dec 2019 | CC BY 4.0 | https://doi.org/10.22541/au.157652715.56884600 | This a preprint and has not been peer reviewed. Data may be preliminary. fti praht nesadn h ikgsbtenlresaeso oe hneadrunoff. and change applicability and cover general snow temperature the scale evaluate air to large cover, between study linkages case snow the a in understanding as variability used to different of magnitude approach is between at patterns the basin this disappearance correlations cover Irtysh investigate including of snow Kaz- The the To catchment, of patterns. of investigate river i) timing pressure catchments Irtysh and to are: atmospheric rates water Upper ii) study depletion main the cover and this snow the of elevations, peak of of sub-basins early/late aims one five of produced timing in in The and present, variability change dataset. cover cover the MOD10A2 snow snow to data MODIS of spring main 2000 2007). the analysis the Riggs, from as using the & data chosen (Hall on akhstan, cover was processing focuses MODIS snow additional study, study of minimal this This archive requiring In and accessible area. methodology study easily robust the (Luojus for an a of regions km provides through mountainous part 25 in it large detection a as cover e.g. form snow source, coarser, which for much unsuitable 2013), is 1 be al., to products and et known the 2013) these are al., of for data microwave et resolution equivalent exist passive water (Luojus data spatial records snow gravimetric product the GRACE and decadal) ‘Globsnow’ though or depth the 2006) snow 2016), (i.e. (Pulliainen, Alternative at Russell, sensors long-term microwave data 2015. and passive no providing in (Wang from launched by However, available AVHRR scales only are the was and datasets time swaths. up first (SWE) weekly MODIS large the opened at of as in has m) legacy satellites m) data (10-20 the Sentinel continues resolution Sentinel-2 (300 Sentinel-3 spatial of resolution while higher availability moderate much 2016), the oldest a al., Recently, the for at et with cover processing 2014). (Hollstein significantly snow additional al., decreases investigating requires AVHRR observations et for but has the (Dietz possibility 2014). present, scales of 2013; sensors the time quality 2012; of to weekly the al., 1978 generation to and et from daily discrimination (Dietz record as cover at Eurasia temporal such snow/cloud and across longest sensors variability pixel) the cover optical represent per snow from data m studying extent (500-1100 for cover Very-High-Resolution employed resolution snow (Advanced been spatial AVHRR leaves on and moderate et and Information (Mashtayeva data, at Spectroradiometer) stations field Radiometer) option. Imaging using meteorological viable resolution undertaken of most realistically (MODerate network be MODIS the sparse cannot as the cover sensing snow and on remote region investigations Kazakhstan means indications East 2016) further al., the provide of would explored. size the which fully However, The be circulation, 2017). to scale atmospheric catchment al., remain large-scale the forecasts, et at of long-range (Zhang follow- retreat effects for cover the monsoon snow of lagged and summer and Ye climate possible Indian anomalies 2015; East-Asian the and temperature the al., of patterns, influence et teleconnection Wegmann to strength between known 2005; the the links also Barlow, controlling with is & by linked retreat (Cohen summer pressure snow been Sea ing spring Siberian Barents-Kara has and still, the Further Eurasian seasons in (AO), different 2017). extent Oscillation Wu, in Arctic ice variability and sea cover mech- (NAO) and cover feedback Oscillation snow patterns Atlantic temperature-snow via Eurasian North patterns the anomalies the circulation temperature 2012). of of atmospheric addition, phases variation al., large-scale In peak to spatial et 2017). of related the (Cohen al., are magnitude Hantel anisms although et Eurasia and 2004; (Gurung across 2017), (Bednorz, timing cover understood al., snow duration well of and et less and prediction Tang is extent the elevation cover 2006; with and snow Mote, relationship 2014) on and 2000; al., control (Kuchment al., et greatest variables et the Kult assessment meteorological exerts 2014; an and Temperature Lee, requires snowmelt further runoff. and variability, models Kang cover runoff of 2007; snow conservation long-term patterns and between Gelfan, and the strategies relationship short- of management of water analysis the spatiotemporal improvement detailed floods, of the The of a analysed mitigation Kazakhstan, ecosystems. the (2016) large all river for about in of al. necessary known duration et is is cover Mashtayeva depletion little snow cover While comparatively and snow rivers, year. depth Kazakh to snow of year of hydrology from distribution the variations for cover Nikiforova, snowmelt snow of and 1990 scale (Kozhakhmetov role and the reported 1967 of floods between spite 42 In flooding over by with affected 2015, º o RC Lnee wno,21) naddition, In 2012). Swenson, & (Landerer GRACE for 2 Posted on Authorea 16 Dec 2019 | CC BY 4.0 | https://doi.org/10.22541/au.157652715.56884600 | This a preprint and has not been peer reviewed. Data may be preliminary. h ewr ogla lps(un,21;Kig ta. 03 ayiae l,21) eprtr ranges Temperature 2017). al., et Malygina capturing 2003; al., Mountains, et +41 Altay Klinge between the 2014; extreme, of (Huang, mm are 1500-2000 slopes presence to Mongolian the up leeward totals by the precipitation affected in resulting significantly and Westerlies is yr the area by transported study moisture Alimkulov the atmospheric 2006; of al., et climate (Hrkal The usage water and water between large over shared Ob conflicts of river, to 2017). the the cascade led of al., for has a joining nature (all et Russia, used transboundary through Russia, Pavlodar and 2014), the Mongolia and fact, (Huang, and enters China, in China Kazakhstan, Kazakhstan, Semey and production; in in power by Shulbinsk Kazakhstan hydroelectric occurs passes and and northern intake Bukhtarma irrigation then Water Ust-Kamenogorsk, in It Mountains, Sea. the 218 above) 2017). namely Kara Altay (length: of reservoirs or al., the city the Kurchum 300,000 into et the Narym, (Bayandinova of flowing of of River eventually region. side Mongolia. downstream population Uba reservoir; administrative western western a Bukhtarma the Kazakhstan the in the by with East into originating on joined flow the streams originate is km) Irtysh of by course (336 Bukhtarma part joined river northwest and are is upper flows km) and basins it the a.s.l into their where of m confluence and China, 2500 the tributaries at before northern river Mountains major Irtysh of Altay The the southwestern uplands of the name the in Kazakh originates through the river and The basin Zaisan. largest Lake the is Ertis Kara southeast. km (13,663 edrvdeeainifrainfo h SE DM(ahkw ta. 01,bten44-55 between 2011), al., et (Tachikawa GDEM ASTER the from information using elevation calculated derived was We dates these and on extent 169 cover (DOY Elevation Snow dates. 2001 (2013). 3.2 adjacent during al. the datasets et on Dietz MOD10A1 based also and interpolation see MOD10A2 snow 81), linear original calculated (DOY the and 2002 in and 2009) present 177) al., material). were et Supplementary gaps Tong (see and 2015; data year layer Few al., sinusoidal and raster et DOY single MODIS (Gascoin each a literature a for into enable the from mosaicked extents in to cover pixel, reprojected reported year, per were previously non-leap m to tiles a 500 similar data of of 40-54 area Raw spacing July the uniform 1). 20th for with (Table extracted – per- WGS84, 2017 February was period UTM45N and 26th validation in snowmelt 2000 to further to between classification grid full year no snow corresponding the each mask, and of 57-201, for lake of 2007), accuracy h24v04 (DOY) analysis a h23v04, Riggs, The year h23v03, & image. using of h22v03, (Hall daily obtained days tiles the each 93% acquired and are on We in as study. two based cloudy reported this first is is in been formed The classification pixel has cover. a Snow product if cloud period). MOD10A1 reported and the the also a is of MOD10A2 ice cover (i.e. index. day lake cloud extent snow any lakes, difference cover while normalized on snow about the present maximum information using is the 1984), aggregation includes provides Anderson, snow temporal & it if down- the (Crane and snow from were algorithm derived ‘snowmap’ composites 2016) as is 8-day Riggs, classified product in & is This cover (Hall Centre. pixel snow product Data daily cover Ice MOD10A1 snow and Snow of 6 National version the MOD10A2 from MODIS loaded the of composites 8-day Cover mm Snow 250 MODIS exceeding 3.1 not Methods rainfall and annual of Sources with downstream dry, Data km very 3 500 is Kazakhstan, basin North river in lower Pavlodar the at Irtysh, Upper in precipitation average an with country, the of resource water main the is km km Kazakhstan, 33.8 East of in flow annual flowing River, Irtysh The Area Study 2 -1 2 aadnv ta. 07 i.)ecmassfiesbbsn,nml b 997km (9,917 Uba namely sub-basins, five encompasses Fig.1) 2017; al., et Bayandinova , bv 0 .. tteIts edaes(hn ta. 08 n eiai ansao odtoson conditions rain-shadow semi-arid and 2018) al., et (Zhang headwaters Irtysh the at a.s.l m 600 above 2 ,Nrm(,5 km (1,852 Narym ), 3 n h otaetdb od Kzyrmt 06.Isuprcthet(196,000 catchment upper Its 2006). (Kazhydromet, floods by affected most the and , ° nsme n -47 and summer in C ° ,80-94 N, 2 ,Krhm(,7 km (4,975 Kurchum ), ° .W rcse erydt sn lu oe neplto algorithm interpolation cover cloud a using data yearly processed We E. ° nwne Mlgn ta. 07.I otatwt high with contrast In 2017). al., et (Malygina winter in C 3 2 n aaEts(4,4 km (143,847 Ertis Kara and ) see Hag 2014). (Huang, Oskemen ¨ 2 rmnrhetto northwest from ) 2 ,Bukhtarma ), see,the Oskemen, ¨ ° and N Posted on Authorea 16 Dec 2019 | CC BY 4.0 | https://doi.org/10.22541/au.157652715.56884600 | This a preprint and has not been peer reviewed. Data may be preliminary. oeatmdli 2hul nlsscce,adw hs toe te enlsspout nve fits of view in products reanalysis other over 0.75 it of chose sampling we grid and fine from cycles, relatively information previous analysis and 2017 with coverage 12-hourly and data temporal observational in the 1990 combining between model in by Forecasting, pressure produced and forecast depletion level is Meteorology a cover sea ERA-Interim for mean 2011). snow Centre and al., European of temperatures et the air (Dee patterns from daily Asia on of central records circulation for ERA-Interim (MSLP) atmospheric downloaded we of area, influence study whole the investigate further To and temperatures air data mean period. were Reanalysis of reference temperatures 3.5.2 records the chose mean (MAM) to We daily available spring relative observations. data; and of anomalies MODIS depth (DJF) 85% with temperature snow winter consistent monthly, calculate than and be obtain less precipitation to to having discarded averaged period we climate further often to reference reason, 1). incomplete, chose our a.s.l.). same (Fig. are we as m the gradient stations, 2000-2017 records For (1186 northwest-southeast these maximum/minimum month. Baitag for a the each and available following as data a.s.l.), are study Mountains m latter temperatures the Altay (827 average the Fuyun in and the use a.s.l.), maximum located of m minimum, are south (737 daily stations Altay located Although Three namely are 2012). basin, stations al., Ertis The et Kara (NO- in (Menne Administration all Network Atmospheric area, and Climatology Oceanic Historical National Global the from AA) observations temperature air obtained We data individual station each Weather for values 3.5.1 calculated also We data MODIS. Meteorological of 3.5 period ranges. elevation composite over 8-day summing the by to basin, due is cover, (1) snow equation is SC Where SCD cover 1). DP snow (equation peak rate when depletion DOY the the as calculate PSCDR (DPSCD) (2). to depletion equation 8 cover to by snow according it peak rate occurs, dividing of depletion depletion and DOY cover the range snow expressed elevation Zhang, similarly peak and We & the basin range. dependent Liu each elevation calculated highly km m for 2014; also is 500 images we in al., cover separate forecasting, expressed et snow each hydrological PSCDR, as (Dietz for for (hereafter and, 2010), studies data basin al., other further each et provide in Parajka for To used 2012; DSCD al., date averaged et then melt and (Dietz We cover free, elevation 2009). snow snow yearon Xie, becomes of of pixel & day concept a Wang the when calculated the 2017; indicates we to which Irtysh, DSCD), similar Upper (hereafter in is disappearance cover cover snow snow in of trends (DOY) potential basin and fluctuations each investigate of variablesTo The cover hypsometry of cells. snow the size grid of grid extracted 2). MODIS we the Calculation Fig. m to GDEM, 3.4 (see 500 corresponding ASTER bins the polygon the elevation a as from m for 100 size information information using on same be areal Based the provide to data. to to MODIS resolution resampled re-vectorized and m then rasterized were 500 were rasters to shapefiles resampled basin and The product. DEM cover large snow single MODIS Basins processed re-projected a 3.3 the then form of were to resolution tiles the The mosaicked with approach. WGS84, consistent neighbour 45N nearest a UTM using to removed artefacts and inconsistencies 80-94 ° attlo 6 niiultlswt 0msailrslto) h E ie eecekdfor checked were tiles DEM The resolution). spatial m 30 with tiles individual 165 of total (a E = = max arg DOY max ( SC DOY ( h,b,DOY ( SC h seeainrange, elevation is 8 ) ( − ,b DOY b, h, SC ( h,b,DOY 2 d -1 ) yietfigtemxmmso oe ieec ewe two between difference cover snow maximum the identifying by ) − 8 ) +8) SC b ( (1) ,b DOY b, h, sbsnadtentto DOY notation the and basin is 4 ° 8)) + x0.75 (2) ° eepoe h al nlssproduct analysis daily the employed We . 8 + n iiinb in 8 by division and Posted on Authorea 16 Dec 2019 | CC BY 4.0 | https://doi.org/10.22541/au.157652715.56884600 | This a preprint and has not been peer reviewed. Data may be preliminary. utos(aaitpuo ta. 05.Ti nlsswsas efre o ahbsna hl n at and whole a as basin fluc- each inter-annual for the isolate performed to also detrended was were analysis data This operation, 2005). this al., 2000 Before influ- between et test. the reanalysis this (Panagiotopoulos assess ERA-Interim temperature To for tuations and and DSCD. used stations anomalies of were from temperature case 2017 Temperatures with the and variables. indices in cover DSCD winter/spring pixel snow with compared with per indices and also and anomalies winter/spring we (r), basins, compared temperatures, and coefficient We of ranges correlation elevation test. ence through separate Pearson’s student temperatures at two-tailed using DPSCD a and relationships and using circulation of (p) strength atmospheric significance variability, the evaluating cover assessing snow analysis, between correlation links investigated We averaging by values mean analysis spring and Correlation standard winter 3.6 and produced mean we 1990-2017 indices, data. the 40-65 all MAM on area For averaging based and month. the by standardized DJF each for calculated and for composites (2005) was MSLP monthly al. SH of et into deviation The Panagiotopoulos data by 2005). reanalysis Siberian outlined al., from as the et obtained quasi-stationary E, coldest calculated (Panagiotopoulos MSLP and the we of hemisphere with semi-permanent Finally, values associated northern a months, daily climate 2017). the high, spring Wu, of early of Siberian and and masses the pattern winter Ye the air of scale throughout 1999; strength Siberia planetary the over al., a stationed expresses et anticyclone which is Clark (SH), AO 2003; index obtained The (Bamzai, high was anomalies. 55 Asia which and height 35 Central mode, between hPa in flow annular zonal 1000 Hemisphere the on Northern to related or based variability (AO), CPC, Oscillation NOAA associated Arctic from commonly the during most vortex included polar also is below-average (weakened) We 2012). POL to enhanced Its (NOAA, an The rise phase Mongolia. reflecting 2007). (negative) giving Siberia, western positive Nakamura, Scandinavia, eastern a and and of over temperatures (Bueh Europe anomalies above-average Eurasia western with anticyclonic central over by over centres characterized primary temperatures weaker a is describes below-average and SCAND phase with The Scandinavia associated positive 2012). commonly over (NOAA, is teleconnection Russia. centre western it primary of a phase anomaly circulation is portions positive main large It its four and for Sea. in anomalies Caspian has and Europe temperature the year pattern in of the EA-WR north temperature throughout and The above-average Eurasia Atlantic months. affecting with west north cover to all China, associated snow east Northern for is from prominent Europe, analyse Scandinavia Atlantic EA centres: most over North to the second the trends of used spanning the precipitation phase centres is the widely positive anomaly positive EA with of been The The dipole track, has 2012). 2003). north-south storm (NOAA, a Gimeno, NAO of and and The consists Bojariu stream and extending 2012). 2004; mode, jet Europe, (NOAA, 40 (Bednorz, north-south over Atlantic phases and Europe anomalies a North over 35 temperature prolonged variability the between average in in Atlantic (below-) of consisting above- Siberia North location to months, over the leading and over winter phase intensity one (negative) during and the positive mode Greenland with over atmospheric associated centred the prominent is one NAO, anomalies, most the of We the pattern specifically dipole Scandinavia 2012). is Eurasia, the (NOAA, (EAWR), NAO of stream pattern The climate Russia jet (POL). Western the pattern the / Polar-Eurasian influence of Atlantic the 90 to intensity East and the – shown and (SCAND) (EA), 20 been position pattern have region the Atlantic that analysis temperature, as East influencing indices the well patterns the in as stream jet tracks included anomalies and storm height waves functions atmospheric hPa and in orthogonal Pre- precipitation 500 changes empirical large-scale Climate to rotated reflect NOAA applied from these the turn, extracted 1987), Livezey, patterns from leading and indices the (Barnston circulation represent atmospheric which monthly Centre, diction hemisphere northern obtained We period. spring monthly, climate to indices reference them the circulation averaged over Atmospheric and anomalies 3.5.3 time, temperature local calculate noon to to values corresponding winter UTC, and 6:00:00 at observations with ° 5 ,adhsbe ieylne oso oe variability cover snow to linked widely been has and N, ° ,80-120 N, ° ° .In N. .It N. ° Posted on Authorea 16 Dec 2019 | CC BY 4.0 | https://doi.org/10.22541/au.157652715.56884600 | This a preprint and has not been peer reviewed. Data may be preliminary. h togs nie:bt h itrA n Haecreae ihtmeaueaoaisfo l three all from anomalies as temperature emerge with tem- SH correlated with and are AO correlation SH their The and at indices. AO looked (MAM) winter first spring the we both and analysis, indices: (DJF) cover strongest winter snow the aggregated for considering indices by suitable peratures, most the anomalies identify temperature To and No indices used. circulation is Atmospheric test 4.2.1 Mann-Kendall the when Analysis basins. level Correlation individual confidence 4.2 for 90% evident the test. is at Mann-Kendall km trend significant the +67 significant only and other of regression is trend linear trend positive least-squares the 0.05) However, ordinary < both (p using significant Irtysh km A PSCDR 5900 Upper PSCDR. over basin whole and Ertis the Kara Ertis 5800 and the km For Kara almost global in (3160 size. the with drop the 2007 resembles greater 2017 large in with closely a and its amount Irtysh was together 2011 to there Upper in ranges, due when for 2010, occurred elevation basin, PSCDR of maxima Ertis 5). individual exception Fig. Kara the not with (see in values, series, catchment larger basin Irtysh basin-wide contributions times Upper smaller the 8 the with show to for a.s.l., value here up m 1500 we is and and reason, 500 ranges, this between 2010, elevation retreat for other the snow except the In by basin controlled from basin. Ertis largely Narym is Kara in itself in 89) PSCDR depletion (DOY later. in snow April week April with of early a synchronous week in smaller occurred first is the occurs it In the DPSCD depletion when 4c). during cover basin, Fig. snow Irtysh and (see peak basins, Upper basin average, 97) whole cross- Uba on (DOY in little and m Uba and most show April 2500-3000 and m in and at Bukhtarma generally m 2500-3000 m occurs between basins ranges 2000 1500-2000 generally e.g. and elevation (< 4b,d,e) DPSCD depletion, basin DSCD, Ertis different basins, snow Fig. Ertis Kara with The peak Kara (see in of early/late As basins. Narym m elevations of 2). a.s.l.) 3500-4000 values lower and contrasting Fig. m the Ertis several (see 1000 at with Kara mainly basin (< correlation, Bukhtarma, DPSCD Bukhtarma between this in earlier lie 500-1000 and of shows 2010 values their a.s.l.) hypsometry 2008 basin-wide in of different while the seen those the ranges, where match be DPSCD elevation to 4a) closely for can due (Fig. to ranges DPSCD basin ranges, seem elevation Kurchum late elevation basins of all two entire exception at of for the seen those basins, DPSCD with be smaller all range, of can elevation the at patterns variability in m the melt inter-annual June However, and not early larger 4). 2500 and does DSCD, (Fig. Between basin or with 3b). Ertis basin, 2005. Fig. comparison Kara in Ertis (see in In basin basin May Kara Uba Bukhtarma in in of average in exception June on July) elevations the the of disappears of upper with in snow end the end 1), At a.s.l., lower the the Table basin. m (until the at Ertis see 3000 At period Kara (mid-April, disappears in observation period. 105 either March) the Uba observation DOY of it in during week the before 2005 a.s.l.), third average during Kara in 73, m on (DOY present in melt (3500-4000 earlier is DSCD disappears completely much DSCD earlier snow and not towards later basins a.s.l.), towards did shift smaller seen and m spike large snow 2008 mostly 1000 isolated a 2003, indicating 2013, (< An shows in in 3c), elevations a.s.l.. also DSCD and Fig. m 2008 early a.s.l., are 1000 (see basins. the m basins and smaller include basin 2000 the 500 features the under between across notable in basin basin patterns Other a.s.l. Ertis Ertis consistent a.s.l.. m Kara m most 2500 in 2000 to The above 3d), above seen appear 2012 s.l.. (Fig. basins best there a basin smaller intervals, 2010, m Ertis the elevation in Kara 3500 in the events larger above of DSCD the seen any late in is in the especially variability elevations, DSCD little lower mean very the in at while trends fluctuations inter-annual strong large notably be no are there While variability cover snow Multiannual the 4.1 in cells grid ERA-Interim Results and 4 station weather each from area. temperatures study with ranges, elevation separate 2 day -1 ,ada vrg foe 50km 4500 over of average an and ), 2 day 6 -1 e erwsietfidfrteUprIts basin. Irtysh Upper the for identified was year per 2 day -1 2 eeautdted o ahbasin each for trends evaluated We . day -1 epciey ihtelowest the with respectively, , Posted on Authorea 16 Dec 2019 | CC BY 4.0 | https://doi.org/10.22541/au.157652715.56884600 | This a preprint and has not been peer reviewed. Data may be preliminary. eet h aeae htsoe oe orlto ihtewne O n eto aeUugri the in Ulungur lake of west and AO, Gobi the winter pixels in the few seen with spring very are correlation The correlations while lower 9c). highest basin, showed The Fig. Ertis elevations. that (see lower Kara area a.s.l. the a.s.l. the m same to m to 1500 the limited (3500 limited and basins, Desert, a.s.l. 1000 mainly smaller the m between the values, ranges, 2000 on elevation in all correlation to Ertis, Across values correlate lower up Kara 9a). strongest seen generally of Fig. the is shows (see with part AO SH Desert most basin), winter south-eastern Gobi with Ertis in the correlation the Kara Mountains in negative of in Altay correlation significant steppes shows the lower strong to dry AO of to of the compared winter south moderate area to the correlations a.s.l. an corresponding with m stronger is side, correlation 2000 Mongolian shows exception below the main DSCD Spatially, values The strongest 9). and basins. the Fig. SH with (see and dependence, fewer ranges in AO elevation elevation significant multiple the or across significant between Kara not DPSCD correlation either in 8b,d). is seen per-pixel Fig. Ertis, correlation again (see basins, The Kara are AO other correlations in the the compared (positive) a.s.l. to In 0.73) highest a.s.l.. compared |r| m the m ranges (max SH, 1500 2000 elevation basin spring to to Ertis elevation regards up Kara different up As basin the Across DPSCD Fig.8a,c). Ertis in 3). (see values with Table others higher and correlation the generally 8 strong to with Fig. basins, to (see Narym Both whole moderate and basins. a Bukhtarma Narym shows basins, as and AO all basin Erys in Irtysh Kara winter in DPSCD Upper ranges, only with with DSPCD correlation above correlate with (negative) correlated also with strongest positively indices 2013 the significantly shows is in AO SH AO Spring winter winter while the negative indices, two the In the and SH DPSCD. positive Among DPSCD negative as and such late spring. and SH occur, following a AO exceptions the the by positive some for followed temperatures variables, a occur average the 2004 ones between with series in positive agreement synchronous all general anomalies and are in the temperature of temperatures anomalies 2008 spite largest and in In The AO DPSCD. temperatures and 2017. the in to anomalies for 2000 values positive from and in contrast, negative AO negative plotted with the mostly are for temperature 2010, is exists Irtysh in spring variability SH Upper interannual the SH), high the anomalies Additionally, while temperature spring (0.94). in temperatures, particularly stations DPSCD cross-correlation, and Altay strong and and AO to ERA-Interim station moderate winter from significant weather show (i.e. variables Altay All and indices 7. Fig. data strongest reanalysis two from the anomalies between 2). variability Table relationship cover (see snow The cells winter at and grid The significant indices limited cells. only and grid circulation is however stations ERA Atmospheric two correlation at 4.2.2 first at anomalies The latter temperature lower temperatures. the winter winter generally while - with is stations, index correlate relationship weather winter also the also the EA of is for and NAO strength except winter SCAND the the AO, although e.g. the cells, temperatures, for grid a spring than or to and stations the winter limited individual to either with is at correlated influence pattern correlation the moderate similar show of indices a extent correlation Other shows the The although ERA-Interim winter. 70 SH, from the between winter band anomalies to and patterns latitudinal compared temperature temperature with east winter spring Fig.7b), between the (see and correlation to area SH ERA- eastern displaced study and between spring temperatures the AO Mountains, between with winter including Altay the correlation Russia, the between significant southern correlation across and of The and (p<0.05) stations 6b,d). Mongolia significant all Fig. northern at is and anomalies Kazakhstan, 2 anomalies Table temperature temperature (see spring spring Irtysh with Upper Interim correlated tip the strongly southernmost in also cells are its grid AO with winter Mongolia, and north and SH temperatures Spring Kazakhstan (see influencing East Mountains winter, 6c). Altay China, in (Fig. the impact Northern China tempe- to local across southeast winter south more over plateau, and with a Tibetan Sea correlated exerts Barents the correlated positively high the of 0.05) Siberian appears to > the AO north Conversely, (p winter influence 6a). non-significantly its the Fig. is Specifically, exerting AO Siberia 6a). the across (Fig. although ratures points data, reanalysis grid the some in at basins across and stations ° n 120 and E ° seFg 6b,d). Fig. (see E 7 Posted on Authorea 16 Dec 2019 | CC BY 4.0 | https://doi.org/10.22541/au.157652715.56884600 | This a preprint and has not been peer reviewed. Data may be preliminary. h rsneo eevisadcanl nCiaadKzksa locue apnn fpa o and flow peak snow of correlating dampening at i.e. attempts causes River, preventing Irtysh also 2014), in the Kazakhstan 2012; of of and al., lack nature et China the regulated (Huang in to downstream The channels due variability 2016). assessed runoff and al., decreased be reservoirs et cannot (Mashtayeva of SWE area presence and study the area product, our covered in snow composite in observations between the streamflow situ relationship Using and the Himalayas. extent study, cover Kush this snow In Hindu cloud-filtered between the Canada. 0.84 in basin, of river basin four correlation Quesnel Gandaki in a betweenthe (2015) identified September the elevations al. (2009) at and in al. 0.78) et April a.s.l. (> et between Delbart correlations Tong m high SCA datasets. 6000 found from SCA several (2017) and discharge al. other in 4000 water et and demonstrated Gurung predicting still, product been in Further catchments. composite has 15% Andean MODIS discharge of uncertainty 8-day stream contribution an or and low found daily SWE a the area, provide using covered calculated to studies DSCD, snow expected as between are recorded area association events be study The these not our However, will MODIS in which disappearance. original elevations melt, SWE. snow snow Higher the the of after respectively. in to week falls elevations, filling first snow higher gap spring the and late data as lower by temperature from at affected situ areas. stem 2002 be remote in also in might and of available might 2001 readily (see use variability often snowfall in the cover not subsequent is product are snow and these accuracy in melt although interpolation uncertainties 2016), snow cover Menzel, of Small cloud & case (Dong on in data improvement biases precipitation and further introduce and 3) a might algorithm point 4); our S1, point cloud-cover although (see S1, the the 2016), snow dependency reduce on Menzel, patchy elevation impact help & small and also Dong enhancing cloud a 2011; can depths by have high scheme al., lower the therefore cloud-interpolation et for of and for (Dietz a SWE uncertainty 39% mapping of areas of related use snow to amount in The for availability. decreasing small a water 94% a 2007) cm, In of represent of 4 assessment 2005). to Riggs, accuracy likely than al., however an & et greater are found (Zhou Hall depths These (2009) cover. streamflow snow average, al. with at et on product can Wang product actually composite (93% and China, composite might the northern snow, product of products in correlation composite and daily conducted higher the clouds study a the of area. to between accuracy of study leading the the occurs also that 2007), on cover, product Riggs, cover than & snow cloud MODIS higher (Hall of for daily impact product be proxy the the 8-day a reduce the in to be to misclassification made propagate can was main depletion product the cover composite assumption snow 8-day While the an and of requires SWE choice also represent The Kazakhstan to discharge. East used river in be and cover hazards can melt cover interpolation. snow area products, flood cloud-cover daily covered 2) between and of and snow variables instead products, association 8-day area that these fact the cover in between snow are and 8-day links DPSCD of variability and Drawing use DSCD cover the derived the 1) snow implies to also of related which are analysis indices the atmospheric and in variables uncertainties main The uncertainty methods and Table Data (see 5.1 basins Uba and Narym Ertis Discussion in temperatures Kara also 5 with in values correlations DSCD high all between Altay; with DSCD, is anomalies, at For correlation temperature 0.79 4). 4). strongest Table spring of the Baitag (see |r| significant: temperatures and basin max. with statistically basin Uba correlation a are significant in with stations for no seen weather basin a.s.l. while is stations, m from Ertis station three 1000-1500 Kara all weather and in at any Fuyun weather correlations seen and from highest from Altay is the anomalies for correlation has a.s.l. a.s.l. basin strongest temperature m this m the 500 spring 500-1000 DPSCD, and i.e. with For Narym band, correlations Baitag. elevation in relevant significant a.s.l. the m show in to 1000 variables stations up to cover seen up 9d). snow is seen Fig. DSCD also Both (see is with basins correlation correlation Uba Significant positive and basin. significant Bukhtarma this Moderate in in 9b). a.s.l. Fig. m (see 2000 basin Ertis Kara southern 8 Posted on Authorea 16 Dec 2019 | CC BY 4.0 | https://doi.org/10.22541/au.157652715.56884600 | This a preprint and has not been peer reviewed. Data may be preliminary. 99 at oe,20) atrso eln nAci e c aebe ikdt h O(i tal., et (Liu AO the mild to unusually linked although been attention, have little ice received sea 2007-2008 Arctic of in winter Entekhabi, decline the & Cohen of 2009-2010, 2003, with patterns to studies, Gimeno, several 2003); Compared & in the Cohen, 2012). (Bojariu reported to the albedo been & anomalies by has the Saito AO wind and initiated the 1999, moisture upward and of was soil increased phases height AO including and SH, of cover mechanisms negative the across snow feedback propagation of autumn highly downward cold strengthening between the and link remarkably the The by warming (2010), fact surface. followed stratospheric al. in October, flux, et in was activity cover Cohen 2009-2010 wave snow to Siberian Winter patterns observation: of According 7). of advance and Asia. (Fig. rapid period anomalies central the depletion temperature during and cover winter record snow Europe SH matching pattern and spring with inverse AO subsequent (negative), similar the of 2009-2010 a both and in and anomalous SH, (positive) highly the 2007-2008 as for out true correlation AO stand is higher winters winter Two opposite shows between the DPSCD correlations while notably, DSCD. The elevation, for a.s.l.: of spring. higher seen patterns m at and is to 1500-2000 AO winter influential below winter most in the significant patterns basin with are circulation Irtysh the DPSCD Upper be and the to anomalies in SH and depletion AO cover the snow shows depletion analysis water cover correlation and snow Bukhtarma Our risks and flood in indices local seen for circulation also implications Atmospheric potential are to 5.3 with sub-basins, appear peaks basins, the not 2011) large operation. Among and does variability; reservoir unresolved. (2000 it for remains multi-annual Uba availability thus which highest and 5), 2017, 2010) the the (Fig. and and of PSCDR show 25% 2000 (2001 in 1), explains Kurchum between Table increase cover trends and (see observed snow significant winter winter the Narym Late of late no year. cause in shows 0 given the 57 it a stations, the be DOY for but weather on SCA of PSCDR, maximum area at in crossing cover for conditions variance proxy snow at melting (DPSCD) a and represent increase of timing PSCDR can between the onset which temperature found with the of was correlated with be (0.50) magnitudes significantly uncorrelated correlation might and not also area were rates are study rates PSCDR including the depletion 2014). sub-basin. for cover al., any trends snow et occur in longer-term peak a (Dietz to study, of accuracy projected, expected this spatial existence as be lower In The would continues with Eurasia. depletion albeit trend cover across data, warming AVHRR snow and using the (2014) peak (1.15 Irtysh investigated al. If and spring Upper et 2011. disappearance Hu the in cover by and in rise snow reported 1979 also greatest earlier between were towards the increased temperatures datasets shift annual with by southern reanalysis average caused from spring, in several 1999, Warming 2015 and using 2018). and and winter al., 1966 1966 et in between between Zhang cover trends Fuyun, records and snow warming depth temperature spring show snow Long-term in spring Altay Siberia. trend late Western upward in over an decrease precipitation identified significant Considering (2003) a investigated. variable al. found the (2014) et was day/year Che (-1 depth & duration snow cover Dai disappearance although snow observation, cover (2016) season of snow melting al. relevant the periods et of during Mashtayeva longer cover of years by snow matching influences Kazakhstan found study in with also the variability their data, multiannual was in over High MODIS (2011) 2010). dominate al. using Kara 2008, et may Asia (e.g. of Dietz central anomalies wind of sub-basin in findings features or largest the cover avalanching topographic with the snow agree other by of in DSCD and in redistribution correlation relevant, Fluctuations variability. snow highest less climatic the shading, regional likely with are aspect. variations 2), as Table temperature spring such (see altitudes, with contributing these basins largest associated the Above most negatively represent of which Ertis. for sub-basins strongly 4), Table all runoff appear (see in variables a.s.l. to DPSCD m Both areas and 1500 below 2017. DSCD elevations in and at fluctuations anomalies 2000 strong temperature between but Irtysh trend significant Upper no the found we depletion study, cover this In snow in trends and Variability discharge. 5.2 and timing and rates depletion covered -1 nteCieeAtybten18 n 01 hl nteO ai,Yang basin, Ob the in while 2011, and 1987 between Altay Chinese the in ) 9 º stem significant A isotherm. C ° e eaeat decade per C Posted on Authorea 16 Dec 2019 | CC BY 4.0 | https://doi.org/10.22541/au.157652715.56884600 | This a preprint and has not been peer reviewed. Data may be preliminary. rnbudr aisusra fBktrarsror npicpe h iigo odn ol ol also could could flooding of timing hydrological non- the ground-based smaller, catchment principle, the the Irtysh in In improve Upper To located reservoir. the stations, Bukhtarma area. at in of study measured forecasting upstream the be flood basins in ideally depletion observations in should transboundary cover AO runoff situ snow Kazakhstan, the in of in of of network ability use lack monitoring predictive possible a the by the flooding. of complicated of subsequent and is assessment and MODIS quantitative melt on agreement, snow the based general abundant above maps this increase to temperature of 2010 led study. and have 2010 spite our 2010), might In in in al, elevations found occurrence et low depletion cover (Cohen at Flood snow snowfalls point peak 7). record late melting with (Fig. very snow winter of in DSCD cold spite Flood late particularly of in Dartmouth February, relatively March, a values (20th as was occurring 2008 early early floods in as and early with reported late and is timing, based however spring) with are to of databases corresponding respect –beginning flooding, (both March with 2018), years in of Observatory, recent seen correspondence (end more also 2017 no in and is has reporting 2015 agreement 2006 the better 2011, Broad in towards in bias news). PSCDR basin a highest Uba local to the third on due in the government be However, PSCDR official might In highest 5). this the 2017. the and although on of and 4 reported timing 2011 (Figs. was the in period 2011 with occurring study mid-April corresponding a series in 2011), shows year Archive basin (Dixinews, 18 PSCDR Uba Active website the peak occurring the news in with Global affecting rates floods Comparison flooding snowmelt and (Fig.5). snowmelt-induced severe peak 2017 2018) particular, to highest and the point al., 2015 with 2018) 2011, agreement, et Observatory, 2010, general (Guha-Sapir 2008, lacking, flooding Flood in are Database modulate (Dartmouth Kazakhstan area to Events Events study throughout the appear Flood Emergency for depletion Large reports the cover of flood snow from Specific peak Kazakhstan. figures eastern of but in rate timing and and be intensity timing can occurrence, in forecasting index variability one flood interannual whether in High and AO 2016), the al., assessed. and et be MODIS (Huang to interplay 5.4 understood the needs entirely 2010), still in al., not that other potential et is evidence the limited Cohen SH of from 1999, a spite the Entekhabi, predicted holds In & and study. it (Cohen AO our anomalies that influence the in AO show between atmospheric negative found relevant also reinforces were SH correlations 2005), a positive lagged al., indeed a relevant to et is temperature no restricted variability, (Panagiotopoulos SH, high as cover spring forecasting, Kazakhstan Siberian snow hydrological the of the on between climate that NAO association the observed the confirming The on of while hypothesis 1999). effect the DPSCD, al., local confirms and et study more (Clark anomalies our and Asia 2013), 2003) western al., (B´aez Cohen, and et actual debate & Europe of the temperature (Saito matter and weaker a NAO winter/spring still the a both are and of with AO AO catchments. connection the the of Eurasian stronger between its forecasts meaning similarity/difference other a cover, long-range physical the and exhibits snow While for AO Irtysh DPSCR/DSCD. fall winter appealing Upper and include the the is anomalies NAO, not in retreat the did both cover to research, analysis snow et Compared future our Foster spring in by and While discussed reported study. AO be between also our winter should autocorrelation was in on and as correlation influence confirmation well latter consistent direct no as This a found possible 1980s, AO. emerged, found the winter/spring but also During (2004), and cover (2013) 2000. cover snow al. al. and snow spring et 1971 spring and between Saito and AO AO study, winter winter winter subsequent snow the between summer and a association cover spring/ In snow an and Eurasian AO. snow fall winter spring/summer 50 between leading between fall/early relationship AO latitudes following winter/spring at the late found DSCD i.e. (2013) leading and found, al. snowmelt et was Foster spring effects Eurasia. observed with lagged over (2003) date correlated Bamzai melt negatively literature. cover is the snow 60 AO in AM between and winter reported influence AO previously the lagged JFM been that between The fact 0.46 anomalies. in of has temperature spring correlation cover influence spring a snow to al., of spring appears and and et modulation DPSCD AO (Ilkka the with the correlated through NAO/AO negatively retreat strongly the cover is AO of snow AO winter phase the 2016). study, positive (Stevenson, our Ni˜na event the In La with a to linked addition Eurasia, in a º ,wieteopst stu ewe 60 between true is opposite the while N, º n 70 and 10 º .I at oe 20) vdnefrreciprocal for evidence (2003), Cohen & Saito In N. º and Posted on Authorea 16 Dec 2019 | CC BY 4.0 | https://doi.org/10.22541/au.157652715.56884600 | This a preprint and has not been peer reviewed. Data may be preliminary. ubrIP\564)amnsee yteRylAaeyo niern U)adaSuetMobility Student a and (UK) Engineering of (project Academy Programme Royal Partnership the Industry-Academia by Al-Farabi administered Newton the IAPP\1516\42) scale. by number catchment supported the was at research further depletion This cover to snow employed modulating be denser in could Acknowledgments A Oscillation approaches 7 strategies. Arctic sensing management the where remote of water catchments different influence informing similar or large the for observations between to assess interactions streamflow, based applied the ground and be into of patterns insights therefore network meaningful depletion can providing cover and runoff, snow of data scale source available validation, dominant of readily Irtysh the lack on the Upper is Despite the snowmelt based approach. for in this is and data of forecasts, runoff approach effectiveness long-term and empirical peak our for feasibility of spring the tool lack the of useful the validation of However, potentially complicates timing schemes. a basin early prevention it or makes flood late early-warning Eurasia relatively of in a parts use predict in to rate index depletion Oscillation cover basins Arctic snow winter winter likely low-lying variability the the larger, of topographic two, ability where the The the basins, in mountain Among smaller especially role. the indices. important DPSCD, in cover High an seen with snow plays are Siberian correlation and correlations spring lower temperatures strongest while with and the (-0.71), correlate Oscillation shows best Arctic Oscillation data that winter reanalysis Arctic patterns and atmospheric the spring stations The are by weather basin. controlled variables by Irtysh are detected Upper disappearance patterns cover the increase atmospheric snow in the regional and of and depletion causes cover anomalies the snow temperature as peak well in research. as fluctuations further trends, Multi-year in longer-term addressed of 5900 existence be 2000-2017 over the should at the hazards, peaked PSCDR, over which flood in trends PSCDR, for clear contrast, relevance In No and their variable. and spring. of mid-March either dates during for between later basin earliest occurs any occurs the km in generally DSCD showing identified were while DPSCD basin period basin, runoff. inter-basin low-lying study the and to largest, inter-annual on contribution the large depending to snowmelt with April, points DPSCD, largest basin and the Irtysh DSCD Upper providing the both in for variability cover differences, of snow drivers of each meteorological analysis in potential The investigate rate patterns. year to depletion depletion of cover cover indices snow snow day circulation observed peak the atmospheric km the 3) depletion, and in and cover stations expressed (DPSCD) snow weather (PSCDR basin peak local year a 2) each in (DSCD), in depletion to from basin used cover disappears basin cover were snow each snow composites, data areal when within cover filtered year maximum Cloud ranges snow of of whole. day elevation MODIS a the m using as 8-day Irtysh disappearance, 500 using cover Upper different snow to out the of in means and timing carried basins the information a was tributary 1) valuable as investigate: analysis major provide area five The covered to the forecasting. hydrology, snow within snow both analysed flood we of of floods. variability region, context snowmelt inter-annual the spring the and in Irtysh, by observations the seasonal impacted runoff of significantly the is course direct understand which upper of Asia, the scarcity Central in the of variability Given basin cover river snow transboundary (2000-2017) large multi-annual a explored PSCDR we study, and this DPSCD In MODIS evaluate on based to Conclusion forecasts means long-term 6 implement a possibly observations providing and based validated, strategies ground management AO. where easily water the areas more to in respect be data, with available could readily products discharge non on it a estimate bands based remains exist, infrared to however is near catchments approach do devised gauged in our sparsely pixels been Since in land also approaches task. and these have water trivial of between algorithms Validation 2015) difference 2017). al., and reflectance al., et images, et the (Tarpanelli (Revilla-Romero on satellite based optical 2016) images through MODIS al., areas from et flooded (Brown detecting by SAR sensing, or remote via investigated be 2 day -1 n21,dsly ekicesn rn o h pe ryhbsnoe h aepro.I view In period. same the over basin Irtysh Upper the for trend increasing weak a displays 2017, in 2 d -1 .I diin eepoe R-nei enlssdata, reanalysis ERA-Interim employed we addition, In ). 11 Posted on Authorea 16 Dec 2019 | CC BY 4.0 | https://doi.org/10.22541/au.157652715.56884600 | This a preprint and has not been peer reviewed. Data may be preliminary. ot tatcOclainadteAci silto nSaSraeTmeauei h Albor´an Sea. the in Temperature Surface Sea the on of Kazakhstan. Oscillation Effects of Arctic Combined Republic the ONE (2013). the and R. and Oscillation Atlantic Ferri-Y´a˜nez, Real, China G´omez-Gesteira,North M., & of htt- available Technology L., F., Republic and Gimeno, People’s regime Engineering C., the the Science, B´aez, J. changing of at in is in Research territories Advanced factors the anthropogenic of in of Journal center flow role International ECM- MOD10A2 river The (2017). Ertis G. the Isakan, prediction of & online. 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(3238), https://doi.org/10.1007/s00376-017-6287-z https://doi.org/10.1038/s41598-018-21637- eoeSnigo Environment of Sensing Remote ora fHydrology of Journal eoeSnigo Environment of Sensing Remote ora fGohsclResearch Geophysical of Journal niomna eerhLetters Research Environmental N.Ise5 January-31 1 5, Issue (No. yrlgclProcesses Hydrological nian .(2015). S. ¨ onnimann, , 371 , yrl Earth Hydrol. 42 1,192– (1), 3,203– (3), , 94 , 195 , (2), 108 , 10 , , Posted on Authorea 16 Dec 2019 — CC BY 4.0 — https://doi.org/10.22541/au.157652715.56884600 — This a preprint and has not been peer reviewed. Data may be preliminary. J-A A .906 .701 .90.36 0.16 0.49 0.56 0.27 0.19 0.68 0.67 0.01 0.43 0.66 0.33 signifi- indicate italics Bold 2017. temperature and MAM 2000 – between 0.54 DJF data (p and ERA-Interim indices correlation 0.69 and (MAM) cant spring station 0.22 and weather (DJF) from winter anomalies average between correlations 2: NAO Table 0.29 0.19 NAO DJF-MAM 0.34 ERA with NAO Correlation ERA with Correlation -MAM MAM ERA with Correlation Baitag at Correlation Fuyun at Correlation Altay at Correlation DJF – DJF Index temperatures – index Correlation shown are Dates data. MOD10A2 composite 8-day for correspondence date year. – non-leap (DOY) a Year for Of Day 1: Table ucu 06 0.37* 0.58 0.42* DPSCD / SH spring Correlation -0.61 DPSCD / AO -0.67 winter Correlation Kurchum -0.48 Ertis Kara Bukhtarma Basin < .5 tidvda ttosEAItrmclsadidcswt ihs correlations. highest with indices and cells stations/ERA-Interim individual at 0.05) H00 00 .2-.202 0.01 0.70 -0.10 0.33 0.20 -0.08 0.23 -0.77 -0.03 0.78 0.14 0.17 0.02 -0.17 0.63 0.06 0.11 0.54 -0.64 -0.22 -0.67 0.08 0.60 -0.13 -0.30 0.36 0.22 -0.13 0.36 0.10 0.11 -0.41 0.14 -0.25 -0.51 0.65 0.02 -0.87 -0.13 0.76 0.07 0.15 0.54 0.38 0.01 -0.12 0.01 -0.29 -0.45 -0.22 0.03 -0.04 -0.77 -0.76 0.39 0.72 0.13 -0.40 0.10 0.20 0.07 -0.31 0.03 -0.48 -0.15 0.24 -0.08 0.04 0.02 -0.79 -0.51 0.69 0.71 0.02 0.42 0.04 SH AO -0.44 POL 0.23 -0.11 -0.01 -0.01 -0.50 0.22 -0.02 0.16 SCAND EAWR -0.83 -0.72 EA -0.03 0.51 -5e 0.15 SH AO -0.03 POL 0.05 0.65 -0.61 0.11 0.46 SCAND EAWR -0.73 EA 0.52 0.24 SH AO POL -0.53 0.53 0.50 SCAND EAWR EA 0-0 00 27/07 – 20/07 19/07 – 201-208 12/07 11/07 – 04/07 192-200 03/07 – 26/06 185-192 25/06 – 18/06 177-184 17/06 – 10/06 169-176 09/06 – 02/06 161-168 01/06 – 153-160 25/05 24/05 – 17/05 145-152 01/05-08/05 137-144 23/04-30/04 121-128 22/04 – 15/04 113-120 105-112 -4 17 .200 00 .30.07 0.23 -0.09 0.07 0.02 i a Avg Max Min Posted on Authorea 16 Dec 2019 — CC BY 4.0 — https://doi.org/10.22541/au.157652715.56884600 — This a preprint and has not been peer reviewed. Data may be preliminary. b 03*-.4 03*-.9-.1-0.48 -0.78 -0.66 -0.91 -0.62 -0.51 -0.76 -0.63 -0.90 -0.70 -0.49 -0.76 -0.63 -0.89 -0.69 -0.34* -0.58 -0.62 -0.71 -0.58 -0.34* -0.62 -0.53 -0.78 -0.71 non-significant marks * Baitag. for a.s.l. m 1000-1500 and Fuyun and Altay cover stations, snow for weather for as DOY band a.s.l. elevation and correlations. m same (DPSCD) the depletion 500-1000 in cover values snow average i.e. peak are DSCD for and (DOY) DPSCD year (DSCD). disappearance of Day stations, weather from (p correlations -0.34* Significant 4: Table -0.61 Uba -0.57 Narym -0.79 Kurchum T MAM Ertis Correlation Kara -0.68 Bukhtarma whole the and basins five the Basin for (DPSCD) depletion cover correlation. snow non-significant peak indicates for * Year area. catchment of Irtysh Day Upper and indices (p correlations (SH) Significant 3: Table b 03*0.18* 0.61 0.47 -0.39* -0.71 -0.60 Irtysh Upper Uba Narym la uu atgAtyFynBaitag Fuyun Altay Baitag Fuyun Altay a < nmle ( anomalies < .5 ewe pig(ac-pi-a,MM eprtr anomalies temperature MAM) (March-April-May, spring between 0.05) .5 ewe itrAci silto A) pigSbra High Siberian spring (AO), Oscillation Arctic winter between 0.05) ° )-DSDCreainMMT MAM Correlation DPSCD - C) 18 a nmle ( anomalies ° )-DSDCreainMMT MAM Correlation DPSCD - C) a nmle ( anomalies ° )-DSDCreainMMT MAM Correlation DPSCD - C) a nmle ( anomalies ° )-DC orlto A T MAM Correlation DSCD - C) a nmle ( anomalies ° )-DC orlto A T MAM Correlation DSCD - C) a nmle ( anomalies ° )-DSCD - C) Posted on Authorea 16 Dec 2019 — CC BY 4.0 — https://doi.org/10.22541/au.157652715.56884600 — This a preprint and has not been peer reviewed. Data may be preliminary. 19 Posted on Authorea 16 Dec 2019 — CC BY 4.0 — https://doi.org/10.22541/au.157652715.56884600 — This a preprint and has not been peer reviewed. Data may be preliminary. 20 Posted on Authorea 16 Dec 2019 — CC BY 4.0 — https://doi.org/10.22541/au.157652715.56884600 — This a preprint and has not been peer reviewed. Data may be preliminary. 21 Posted on Authorea 16 Dec 2019 — CC BY 4.0 — https://doi.org/10.22541/au.157652715.56884600 — This a preprint and has not been peer reviewed. Data may be preliminary. 22