Skip to main content Accessibility help


  • Access


      • Send article to Kindle

        To send this article to your Kindle, first ensure is added to your Approved Personal Document E-mail List under your Personal Document Settings on the Manage Your Content and Devices page of your Amazon account. Then enter the ‘name’ part of your Kindle email address below. Find out more about sending to your Kindle. Find out more about sending to your Kindle.

        Note you can select to send to either the or variations. ‘’ emails are free but can only be sent to your device when it is connected to wi-fi. ‘’ emails can be delivered even when you are not connected to wi-fi, but note that service fees apply.

        Find out more about the Kindle Personal Document Service.

        Compilalion of long-term glacier-fluctuation data in China and a comparison with corresponding records from Switzerland
        Available formats

        Send article to Dropbox

        To send this article to your Dropbox account, please select one or more formats and confirm that you agree to abide by our usage policies. If this is the first time you use this feature, you will be asked to authorise Cambridge Core to connect with your <service> account. Find out more about sending content to Dropbox.

        Compilalion of long-term glacier-fluctuation data in China and a comparison with corresponding records from Switzerland
        Available formats

        Send article to Google Drive

        To send this article to your Google Drive account, please select one or more formats and confirm that you agree to abide by our usage policies. If this is the first time you use this feature, you will be asked to authorise Cambridge Core to connect with your <service> account. Find out more about sending content to Google Drive.

        Compilalion of long-term glacier-fluctuation data in China and a comparison with corresponding records from Switzerland
        Available formats
Export citation



Data on world-wide glacier fluctuations are being compared and interpreted in an increasing number of publications (Patzelt, 1985; Kislov and Koryakin, 1986; Makarevich and Rototayeya. 1986; Vallon and others. 1986; Haeberli and others. 1989a; Kick, 1989; Oerlemans and others. 1993; Williams and Ferrigno, 1993; Oerlemans, 1994). The surface areas of glaciers in China account for about 10% of the total surface area covered by ice caps and mountain glaciers on Earth, existing outside the large polar ice sheets (Haeberli and others, 1989b. With the exception of a few individual glaciers, however, most Chinese glaciers have been rarely monitored and measured. Consequently, data on glacier fluctuations in China are limited. The Chinese glacier monitored and measured in most detail is Ürümqi Glacier No. 1 within the Ürümqi River source region in the central Tien Shan. Since 1980. variations in the positions of glacier fronts (length change) during various time periods have been reported for anout 200 glaciers (Zhang, 1980a. b: Karakoram; Zhang and Mi. 1981: Qilianshan, Kunlunshan and Tien Shan; Wu and Others, 1983: Tien Shan; Wu and others, 1985: Qilianshan, Kunlunshan and Tien Shan; Wu and others, 1983: Tien Shan; Xie and Others, 1985: Qilianshan;; Ren, 1987: Kunlunshan; cf. also Shi and others, 1988. cf. Fig. 1). Glaciers in the Swiss Alps were chosen for a main comparison, because they have been monitored in considerable detail during the past century. In Switzerland, mass-balance information exists for five glaciers and extensive records on length change are available for more than 100 glaciers.

Fig. 1 Location of areas studied (inset) and of mountain ranges in China. The number of glaciers studied is: 55 in Tien Shan. 42 in Qilianshan, 40 in Kunlunshan, nine in the Himalaya, seven in Hengduanshan, six in the Karakoram. three, in Tanggulashan and Iwu in lite Altai.

Glacier Mass Balances

Although Ürümqi Glacier No. 1 has been measured and studied in detail, mass-balance observations were interrupted between 1967 and 1979. The mass-balance data used here for the time interval 1967–79 were reconstructed by J. H. Zhang (1981), Zhang and others (1984) and Shi and others (1988) on the hasis of precipitation and air temperature recorded by a meteorological station situated 2.5km from the glacier and at an altitude of 3589ma.s.l. The mass-balance record of another glacier. Qiyi Glacier in the central Qilianshan, was reconstructed (Liu and Xie, 1987) after 5 years of field measurements using a relationship between accumulation, ablation and meteorological parameters (altitude of the 0°C isotherm, summer air temperature, etc.). Both glaciers are in areas of a continental climate. In Switzerland, the mass balance of Aletschgletscher has been estimated from a hydro-logical balance model calibrated by precision mapping in 1927 and 1957. The model uses predpitadon and run-off measurements and assumes that annual evaporation remains constant.

Figure 2 Compares annual mass balances since 1959 for glaciers in China and Switzerland. Annual variations in mass balance are quite synchronous for the Swiss glaciers, which are located in the same climatic region and are close together. On the other hand, short-term variations are not synchronous in Switzerland and China. Letrèguilly and Reyuaud (1990) discussed similar spatio-temporal patterns of mass-balance variability and pointed out that the identity of annual mass-balance variations cannot be recognized beyond individual mountain ranges. They further concluded that, beyond a distance of 500 m, synchroncity cannot be found at decadal time-scales but dial the main secular trends seem to be common in Europe and High Asia. Close inspection of the records indicates that common negative balances during 1962–64 in Switzerland, for instance, correspond to highly positive balances of Ürümqi Glacier No. 1. An abrupt change to positive balances on Swiss glaciers since 1965. and continuing until about 1970. is accompanied by strong mass losses of Ürümqi Glacier No. 1.

Fig. 2 Specific net mass balance (mm w.e.) for glaciers in Switzerland and China. (a) Swiss glaciers: Silveretta-gletscher (solid line), Limmerngletscher (dotted line), Griesgletscher (dashed line) and Aletschgletscher (dashed) dotted line); (b) Ürümqi Glacier No. 1 in China.

Figure 3 shows time series of cumulative-balance variations. There is considerable variation among individual glaciers with respect to overall gain or loss in mass. Even though the reconstructed mass balance for Qiyi Glacier is very approximate, evidence of overall mass gain can be found. Four of the five annual mass balances determined in the field were positive and the average equilibrium-line altitude on the glacier decreased by about 100m between the decade 1957–66 to the decade 1967–77 (Ding and Kang, 1985). The tendency towards a positive cumulalive balance for Qiyi Glacier could therefore be real. In Switzerland, cumulative balances since 1960 were slightly positive on Silvrettagletscher and markedly negative on Griesgletscher. The phenomenon of highly variable cumulative mass-balance series and significantly different conditions of health appears to be common for glaciers in the Nothern Hemisphere (Letrèguilly and Reynaud, 1990). Amongst the reasons for this are the orientation of the glaciers and the distribution of glacier area with altitude (hypsometry). In Switzerland, mass balances a ppear to be more negative on glaciers that are exposed to the northeast (there appears to be a similar phenomenon for most glaciers in France and Austria; cf, the data given in Haeberli. (1985), Haeberli and Müller (1988); Haeberli and others (1994); Haeberli and Hoelzle (1995)). Unfavourable orientations of glaciers in the Tien Shan with respect to the predominant humidity source are the northeastern and southeastern quadrants (Table 1), Qjyi Glacier, however, has an unfavourable exposure but a positive mass balance. Glacier orientation, therefore, cannot be the only or even lhe most important factor influencing the variability in cumulative mass balances. The highly positive balance of Qiyi Glacier could result from its hypsometry (Fig. 4); the wide firn basin is favourable for the accumulation of snow. In a comparable way, a relatively large firm basin seems to remedy the unfavourable northern exposure of Silvrettagletscher. Plallalva-gletscher and Limmerngletsehcr are probably typical examples of the combined elfecls of orientation and hypsometry. These two small glaciers are immediately adjacent to each other but their mass balances are different. Their combined exposure and hypsometry may explain the different balances. A similar phenomenon can also be observed with Hinlereis- and Kesselwandferner in Austria (Kuhn and others, 1985; Greuell, 1992).

Fig. 3 Cumulative mass balance (CMB) vs time for glaciers in (a) Switzerland and (b) China.

Table. 1. Relationship between orientation of accumulation area and cumulative balance

Fig. 4 Hypsometry of glaciers with negative (left) and positive (right) cumulative mass balance. Ordinate gives altitude interval in m a.s.l.

In strong contrast to the remarkable scatter in annual and cumulative mass balance, changes in cumulative mass balance are similar over the time period considered (1959–90): during the lalesi decade (1980–90), an accelerating trend towards more negative mass balances appears in both regions (Fig. 3). Short-term local to regional variability is nevertheless superimposed on this general trend. A change towards markedly negative balance for Ürümqi Glacier No. 1 occurred in 1978 with the strongest loss in 1981 (Fig. 2), while Swiss glaciers at the same time maintained positive or zero balances. Rates of mass loss Ibr the Swiss glaciers, on the other hand, have accelerated strongly since 1981. The trend towards negative balances then remains obvious for the entire decade of the 1980s in both regions. This observation may indicate that accelerated warming of the 1980s, as reflected by glacier and permafrost changes in the Alps (Haeberli, 1994), not only appears in mountain ranges with transitional to maritime climatic conditions but also affects areas of strong continentality.

Variations in the Positions of Glacier Fronts (Glacier-Length Changes)

There are no continuous data on annual variations in the positions ol glacier fronts in China. Information on glacier-length changes over various longer lime intervals, however, is available in a number of publications (Zhang, 1980a, b; Zhang and others. 1981; Wu and others, 1983; Haeberli, 1985; Xie and others, 1985; Ren, 1987; Haeberli. 1988; Shi and others. 1988; Haeberli and Hoelzle. 1993). With the exception of a few direct measurements, most of those data were obtained from topographic maps at scales of 1 :50000 and 1 : 100000, from aerial photographs and from satellite imagery. Data on glacier-length changes in Switzerland were mainly extracted from the annual reports prepared by VAW/ETHZ for the Swiss Glacier Commission (Kasser and others, 1986; Aellen, 1988; Aellen and Herren, 1991, 1992a, b, 1993). Most of the time intervals considered are shorter than die dynamic response time of the glaciers involved. It is, therefore, necessary to analyse cumulative length changes of glaciers with comparable geometry especially total length) in order to avoid comparing glaciers with highly different response characteristics (cf. Kuhn, 1978; Haeberli and others, 1989a; Haeberli, 1995).

Figure 5 compares cumulative length changes of three Chinese glaciers with average cumulative length changes determined for Swiss glaciers of more or less equal length. Tuergangou Glacier (Tien Shan) and Qiyi Glacier (Qilianshan) are continental glaciers but Hailuogou Glacier (Mount Gonga in the Hengduanshan) is some-whal maritime. These three glaciers are among the few in China which have been documented by repeated surveys over variable time intervals and hence may be compared with detailed Swiss records. A general trend towards retreat has obviously predominated during the past 30 years for the investigated glacier sizes in China as well as in Switzerland. It is also noteworthy that the continental Qiyi Glacier reacts less and the maritime Hailuogou Glacier more sensitively than Alpine glaciers with their transitional climate.

Fig. 5 Comparison between average change in length of Swiss glaciers and changes in length of individual Chinese glaciers.

The similarity of long-term glacier-length changes in China and Switzerland also appears in the statistics for different classes of glacier length (Table 2). Increases and decreases in the percentage of retreating glacier snouts during different time intervals roughly follow the same pattern in both countries, especially with respect to glaciers shorter than 10km. Glacier retreat clearly predominates, with the exception of the intermittent advance of long Chinese glaciers after the middle of the present century and during the period around 1980 when 2–5 km long glaciers advanced in both countries. In general, percentages and rates of retreat for glaciers shorter than 10km were higher during the 1950s but decelerated since the 1960s, leading to a tendency towards İntermittent advance in the 1970s with a peak from the middle of the 1970s to the beginning of the 1980s.

Table. 2. Comparism of length changes for comparable length classes (km) of glaciers in China and Switzerland (% is percentage of retreating glaciers with number of glaciers in brackets; rate is average rate of length change in ma −1 for the entire sample of the size category and the considered time interval). The locations of the Chinese glaciers for the individual time intervals are as follows: (10 = Qilianshan (eight glaciers); (2) = Tien Shan (two glaciers) and Qilianshan (one glacier; (3) Qilianshan (nine glaciers); (4) Qilianshan (four glaciers) and Tien Shan (three glaciers); (5)Qilianshan (six glaciers), Tien Shan (one glacier) and Kunlunshan (seven glaciers); (6)Qilianshan (two glaciers) and Nianqingtanggulashan (one glacier); (7) Qilianshan (four glaciers) and Altaishan (one glacier); (8) Qilianshan (11 glaciers), Tien Shan (11 glaciers) andKunlunshan (six glaciers); (9) Tien Shan (one glacier), Pamir (one glacier) and Kuntunshan (four glaciers); (10) Tien Shan (two glaciers) and Hengduanshan (one glacier); (11) Qilianshan (one glacier). Karakoram (four glaciers), Himalaya (one glacier) and Henduanshan (two glaciers); (12) Tien Shan (11 glaciers); (13) Qilianshan (one glacier), Tien Shan (11 glaciers), Kunlunshan (17 glaciers), Karakuram (two glaciers) and Himalaya (one glacier); (14) Qilianshan (one glacier), Tanggulashan (one glacier). Kunlunshan (two glaciers) and Hengduanshan (four glaciers); (15) Qilianshan (one glacier), Karakoram (one glacier). Hengduanshan (two glaciers); (16) Tien Shan (six glaciers); (17) Qilianshan (one glacier). Tien Shan (two glaciers). Kunlunshan (ten glaciers), Himalaya (one glacier) and Karakoram (one glacier); (18) Qilianshan (one glacier). Tanggulashan (one glacier), Hengduanshan (three glaciers) and Kunlunshan (one glacier)

The retreat of the Chinese glaciers longer than 10 km during various time periods appears to be less steady and less homogenous than in Switzerland. In fact, there seems to be a distinct difference between the two countries with respect to the average rates of glacier-length changes and to percentages of advance/retreat for large glaciers. One reason may he that 51 Chinese glaciers with lengths exceeding 10 km. including 18 glaciers longer than 20 km, are used for the analysis, whereas there are only five Swiss glaciers longer than 10km and only one (Aletsch-gletscher) longer than 20 km. Another reason may be the larger errors for glaciers in China, because data on length changes of large glaciers in China are mostly estimated from satellite imagery with resolutions and accuracies of about 100 m. Comparing percentages of retreating glaciers therefore may be more representative in this special case of large glaciers and indeed gives somewhat similar results for both regions.

Figure 6 summarizes percentages of advance/retreat for all glaciers monitored in China and Switzerland over decadal time intervals. Historically, this approach has been popular. It is, however, highly problematic, because of the different response types involved and can, at best, give only a very general outline. Because of the somewhat steady retreat for large glaciers. Figure 6 shows principally decadal reactions of smaller glaciers and, as such, tends to confirm the similarity of glacier changes in both countries beyond the time-scale of one or a few years.

Fig. 6 Variation in the position of fronts for about 200 glaciers in China and 160 glaciers in Switzerland.

Fig. 7 Relationship between cumulative mass balance (CMB) and cumulative length change (CLC) for glaciers of different lengths.

Relation between Mass Balance and Glacier-Length Changes

The reactions of glaciers to climatic change involve a complex chain of processes. Mass balance is the direct, undelayed consequence of climatic forcing, while the length change is an indirect, delayed reaction. The fluctuatins described above for smaller glaciers in both countries demonstrate their sensitive reactions to climatic change. Actually, length reactions to mass-balance forcing for small glaciers are very quick (Fig. 7). Length changes for the small Plattalvagletscher, for instance, are almost synchronous with balance variations and the curve of (cumulative) glacier-length changes is not much smoother than the one of cumulative mass balance. Almost synchronous changes in length and mass balance can also be found over various time intervals at Ürümqi Glacier No. 1, though its length changes have not been continuously measured. With increasing glacier length, tongue reactions seem to be slower and the smoothing of curves from cumulative length change with respeel to mass-balance records are more pronounced. For Silvretta-gletseher, synchronous variations still exist but are less obvious. No short-term (yearly to multi-annual) relation between length change and mass balance exists for Aletsch-glctscher, a glacier more than 20km long. Its reaction time, i.e. the time lag between a marked change in cumulative mass balance and the onset of lhe corresponding advance/retreat of the glacier snout, may be 30 years or more; time for full dynamic response and adjustment to a new equilibrium length is estimated at about 70–80 years (Haeberli, 1994; Haeberli and Hoelzlc, 1995). Such long delays will essentially smooth out shorl-lerm effects of climate and mass-balance forcing on glacier-length changes, so that yearly to decadal glacier-terminus reactions to climatic change will be unclear.

Figure 8 summarizes the relation between mean mass balance and mean annual length change four length classes of Swiss glaciers. The length changes for the shortest glaciers (≤2km) are indeed almost perfectly synchronous with variations in mass balance. Length changes for larger glaciers (total length = 2–5 km and 5–10km) appear to follow after a time lag of a few years. The length changes for 5–10 km long glaciers have a slightly longer time lag combined with more pronounced smoothing but the differences with respect to the 2–5 km long glaciers are too small to make sharp distinctions. Interpretation of the length-change signal of glaciers longer than 10km and for the time interval covered by direct mass-balance measurements is more difficult. Reaction times are most likely to be in the decade range. Most remarkably, however, and in contrast to the shorter glaciers, average rates of change remained negative (retreat) throughout the observation period. The longest glaciers were not (yet?) able to re-advance as a reaction to the positive mass balances in the late 1960s and late 1970s.

Fig. 8 Comparison between annual mass balance and annual length change for various sizes of Swiss glaciers; (a) 5 year centred moving average of mass balance; (b) 5 year centred moving average for length changes in different length (L) classes.

The time period considered in Figure 8 is about 30 years and, hence, shorter than the characteristic dynamic response time of most mountain glaciers. By looking at lime intervals, which correspond to the dynamic response time (ta) of individual glaciers, the long-term mean mass balance (〈b〉) can be inferred from cumulative length change caused by a step change in mass balance (δb) on the basis of assumed steady-state conditions before and after response, linear adjustment of mass balance to new equilibrium conditions during response and continuity (cf. Johannesson and others, 1989; Haeberli, 1990, 1994; Haeberli and Hoelzle, 1995, for background and calibration):




where bt , is the (annual) ablation at the glacier terminus, δb is the assumed Step change in mass balance leading to the length change δL over the time period ta starting from the original glacier length L0 and hmax is maximum glacier thickness (all values in water equivalent).

Table 3 comparts average mass balances calculated in this way for the Alpine Rhonegletscher and the Chinese Ürü mqi Glacier No. 1. The agreement between the directly measured mass balance and the mass balance inferred from cumulative length change is striking for Rhonegletscher (measured: −0.25/inferred: −0.28 m w.e. year−1 as well as for Ürümqi Glacier No. 1 (measured: −0.14/inferred: −0.11 m w.e. year−1). The dynamic response time of Rhonegletscher is about twice as long as that of Ürümqi Glacier No. 1. For direct comparison of the two glaciers and their secular mass changes inferred from cumulative lengih change, equally Umg time intervals should be considered. Ürümqi Glacier No. 1 began to retreat from its Little Ice Age maximum in 1876; by 1990, it had lost 0.5 km in length. With this historical retreat, the secular balance change (δb) and average secular balance (〈b〉) calculated from Equation (2) become −0.8 and −0.4 m w.e. year−1, respectively. However, the glacier was probably able to adjust fully twice or even three times as a reaction to (assumed step-type) mass-balance changes since the end of the Iasi century. The calculated secular mass-balance changes and average secular mass-balance values must, therefore, be reduced correspondingly. The resulting average secular mass loss of Ürümqi Glacier No. 1 is 0.1–0.2 m w.e. year−1. Such a value is roughly half the characteristic values obtained for Alpine glaciers (Rhonegletscher in Table 3; cf. also the data given by Haeberli (1994) and Haeberli and Hoelzle (1995) — a fact which may be explained by the lower climatic sensitivity of the continental-type Ürümqi Glacier No. 1. It is especially important to note that the cold firn area of Ürümqi Cilacier No. 1 (Haeberli and others, 1994) probably reacted to 20th-century atmospheric warming by increased mellwater relreezing and firn warming; mass loss was therefore restricted to the ablation area or about half the glacier area. Characteristic rates of secular glacier mass loss are in any case in the range of dm year−1 and, hence, closely comparable in both regions.

Table.3. Comparison of measured and estimated glacier mass changes. Sources: Aellen (1981), Wang (1981), Zhang. Z.S. (1981), Funk (1985), You (1988), Chen and Funk (1990), Haeberli and Hoeizle (1995)


Effects of climatic forcing on glaciers are different during various time periods and strongly depend on topographic and glaciological factors. Variations in the mass balance of individual glaciers at present depend mainly on humidity conditions and topographic factors (hypsometry and orientation with respect to the main humidity source). Comparisons between glacier evolution in China and the Swiss Alps nevertheless demonstrate that some characteristics of glacier fluctuations are similar in both regions during past decades. The overall trend is one of mass loss and glacier retreat with a modest intermittent growth and re-advance between 1970 and 1980. The similarity of variations in the positions of glacier fronts between the two countries points to comparable climatic forcing over decadal time intervals on the Eurasian continent. Inter-annual variations in mass balances, however, are different and remain partly unexplained. Further investigation of such differences is necessary and intercomparison of glacier fluctuations should be expanded to other regions of the world.


The work of Y.J.D. was funded by the Chinese Academy of Sciences while this author visited VAW/ETH Zürich during 1993–94. M. Aellen. Η. ösch, M. Hoelzle and Α. Kääb at VAW/ETH Zürich assisted with data management and critically read the manuscript.

4 February 1996


Aellen, M. 1981. Recent fluctuations of glaciers. In Kasser, P. and Haeberli, W., eds. Switzerland and her glaciers: from the ice age to the present. Zürich, Swiss NationalTourist Office (SNTO) and Kümmerly adn Frey, 7089.
Aellen, M. 1988. Die Gletscher der Schweizer Alpen 1979/80 und 1980/81. Les variations des glaciers suisses 1979/80 et 1980/81. Zürich, Gletscherkommission der Schweizerischen Naturforschenden Gesellschaft. (Glaziologisches Jahrbuch, Bericht 101 and 102.)
Aellen, M. and Herren, E.. 1991. Die Gletscher der Schweizer Alpen 1981/82 und 1982/83. Les variations des glaciers suisses 1981/82 et 1982/83 Zürich, Gletscherkommission der Schweizerischen Akademie der Naturwissenschaften. (Bericht 103 and 104.)
Aellen, M. and Herren, E.. 1992a. Die Gletscher der Schweizer Alpen 1983/84 und 1984/85. Les variations des glaciers suisses 1983/84 et 1984/85 Zürich, Gletscherkommission der Schweizerischen Akademie der Naturwissenschaften. (Bericht 105 and 106.)
Aellen, M. and Herren, E.. 1992b. Die Gletscher der Schweizer Alpen 1985/86 und 1986/87. Les variations des glaciers suisses 1985/86 et 1986/87 Zürich, Gletscherkommission der Schweizerischen Akademie der Naturwissenschaften. (Bericht 107 and 108.)
Aellen, M. and Herren, E.. 1993. Die Gletscher der Schweizer Alpen 1987/88 und 1988/89. Les variations des glaciers suisses 1981/82 et 1982/83 Zürich, Gletscherkommission der Schweizerischen Akademie der Naturwissenschaften. (Bericht 109 and 110.)
Chen, J. and Funk, M. 1990. Mass balance of Rhonegletscher during 1882/83–1986/87. J. Glaciol., 36 (123), 199209.
Liangfu, Ding and Xiancheng, Kang. 1985. [Climatic conditions for the developent of glaciers and their effect on the characteristics of glaciers in Qilian Mountains.] Lanzhou Institute of Glaciologh and Cryopedology. Memoirs. Academia Sinica, 5 915. [In Chinese.]
Funk, M. 1985. Räumliche Verteilung der Massenbilanz aff dem Rhonegletscher und ihre Beziehung zu Klimaelementen. Zürcher Geogr. Schr. 24.
Greuell, W. 1992. Hintereisferner, Austria: mas-balance reconstruction and numerical modelling of the historial length various. J. Glaciot., 38 (129), 233244.
Haeberil, W. 1985. Comp. Fluctuations of glaciers 19675–1980 (Vol. IV). Paris, International Commission on Snow and Ice of the Intrnational Association of Hydrological Sciences/UNESCO.
Haeberli, W. 1990. Glacier and permafrost signals of 20th-century warming. Ann. Glaciol., 14, 99101.
Haeberli, W. 1994. Accelerated glacier and permafrost changes in the Alps. In Beniston, M. ed. Mountain environments in changing climates. London and New York, Routledge, 91107.
Haeberli, W. 1995. Glacier fluctuations and climate change detection—operational elements of a worldwide monitoring strategy. WMO Bull., 44 (1), 2331.
Haeberli, W. and Hoelzle, M., Comps. 1993. Fluctuations of glaciers 1985–1990 (Vol. VI). Wallingford, Oxen, IAHS Press; Nairobi, UNEP; Paris, UNESCO.
Haeberli, W. and Hoelzle, M.. 1995. Application of inventory data for estimating characteristics of and regional climate-change effects on mountain glaciers: a pilot study with the European Alps. Ann. Glaciol., 21, 206212.
Haeberli, W. and Müller, P. comps. 1988. Fluctuartions of glaciers 1980–1985 (Vol. V). Wallingford, Oxen, IAHS Press; Nairobi, UNEP; Paris, UNESCO.
Haeberli, W., Müller, P. Alean, P. and Bösch, H. 1989a. Glacier changes following the Little Ice Age—a survery of the intrnational data basis and its perspectives. In Oerlemans, J., ed. Glacier fluctuations and climatic change. Dordrecht, ets., Kluwer Academic Publishers, 77101.
Haeberli, W., Bösch, H. Scherler, K., Østrem, G. and Wallén, C. C. eds. 1989b. World Glacier Inventory: status 1988. A contribution to the Global Environment Monitoring System (GEMS) and the Internationl Hydrological Programme. Wallingford, Oxen, IAHS Press; Nairobi, GEMS-UNEP; Paris, UNESCO.
Jóhannesson, T., Raymond, C. and Waddington, E., 1989. Time-scale for adjustment of glaciers to changes in mass balance. J. Glaciol., 35 (121), 355369.
Kasser, P., Aellen, M. and Siegenthaler, H.. 1986. Die Gletscher der Schweizer Alpen 1977/79. Les variations des glaciers suisses 1977/78 et 1978/79. Zürich, Gletscherkommission der Schweizerischen Naturforschenden Gesellschaft. (Glaziologisches Jahrbuch, Jubiläumsband 99 und 100.)
Kich, W. 1989. The decline fo the last Little Ice Ajge in high Asia compaed with that in the Alps. In Oerlemans, J., ed. Glacier fluctuations and climatic change. Dordrecht, etc., Kluwer Academic Publishers, 129142.
Kislov, A.V. and Koryakin, V.S.. 1986. Prostranstvennyye i vremennyye zakonomernostic izmeneniy lednikov Yevraziyskoy Arktiki/Spatial and temporal regularities of glacier fluctuations in Eurasiand Aretic. Mater. Glyatsiol. Issled, 57, 120–125 (Russian); 236241 (English).
Kuhn, M. 1978. Correspondence. On the non-linearity of glacier length respnse to climatic changes: comments on a paper by H. W. Posamentier. J. Glaciol., 20 (83), 443446.
Kuhn, M., Markl, G., Kaser, G., Nickus, U., Obleitner, F. and Schneider, H.. 1985. Fluctuatons of climate and mass balance: different response of two adjacent glacirs. Z. Gletscherkl. Glazialgeol., 21, 409416.
Letréguilly, A. and Teynaud, L.. 1990. Space and time distribution of glacier mass-balance in the Northern Hemisphere. Arct. Alp. Res., 22 (1), 4350.
Chaohai, Liu and Zichu, Xie. 1987. [A primary study of the relationship between glacier mass balance and climate in the “July First” glacier.] J. Glaciol. Geocryol., 9 (4), 301310. [In Chinese with English summary.]
Makarevich, K.G. and Rototayeva, O. V. 1986. Sovremennyye klebaniya gornykh lednikov severnogo polushchariya/Present-day fluctuations of mountain glacirs in the Northern Hemisphere. Mater. Glyatsiol. Issled. 57, 2533 (Russian); 157163 (English).
Oerlemans, J. 1993. A model for the surface balance of ice masses: part I. Alpine glaciers. Z. Gletscherkd. Glazialgeol., 27/28, 1991/1992, 6383.
Oerlemans, J. 1994. Quantifying global warming from the retreat of glaciers. Science, 264 (5156), 243245.
Patzelt, G. 1985. The period of glacier advances in the Alps, 1965 to 1980. Z. Gletscherkd. Glazialgeol., 21, 403407.
Binghui, Ren 1987. [Some factors of development for glaciers in Kunlun mountains and their advance and retreat.] In Proceedings, Second National Conference on Glacilogy. Gansu Press, 7583. [In Chinese.]
Reynaud, L. 1993. Glaciers of Europe—glaciers of the Alps. The French Alps. U.S. Geol. Surv. Prof. Pap. 1386-E, E23–E36.
Yafeng, Shi, Maohuan, Huang and Binghui, Ren. 1988. [Recent fluctuations of glaciers in China.] In Shi, Yafeng, Huang, Maohuan and Ren, Binghui, eds. An introduction to glaciers in China. Beijing, Science Press, 171184. [In Chinese.]
Vallon, M., Reynaud, L. and Letréguilly, A. 1986. Glacier mass balance reconstructions for the Northern Hemisphere covering the Past century and their climatic significance. Mater. Glyatsiol. Issled. 57, 153157.
Jingtai, Wang 1981. [Ancient glaciers at the head of Ürümqi river, Tien Shan.] G. Glaciol. Geocryol., 3, Special Issue, 5763. [In Chinese with English summary.]
Williams, R.S. Jr, and Ferrigno, J.G., eds. 1993. Satellite image atlas of glaciers of the world. Europe. U.S. Geol, Surv,Prof.Pap. 1386-E.
Guanghe, Wu, Shunying, Zhang and Zhongxiang, Wang. 1983. [Retreat and advance of modern glaciers in Bodge, Tian Shan.] J. Glaciol. Geocryol., 5 (3), 143152. [In Chinese with English summary.]
Xie Zichu, G. H. Wu and Wang, Liun 1985. [Recent advance adn retreat of glaciers in Qilian Mountains.] Lanzhou Institute of Glaciology and Cryopedology. Memoirs. Academia Sinica, 5, 8290. [In Chinese.]
Genxiang, You 1988. [Map of Glacier No. 1 and No.2 at the Ürümqi river, Tianshan.] Xian, Cartographic Publishing House. (Scale 1: 4,000.)
Jinhua, Zhang 1981. [Mass balance studies on the No. 1 Glacier of Ürümqi river in Tianshan.] J. Glaciol. Geocryol., 3 (2), 3240. [In Chinese with English summary.]
Jinhua, Zhang Xiaojun, Wang and Jijun, Li. 1984. [Study on reationship between mass balance change of Glacier No.1 at the headwater of Ürümqi river, Tianshan and climate.] J. Glaciol. Geocryol., 6 (4), 2536. [In Chinese with English summary.]
Xiang-Song, Zhang 1980a. [Advancing and retreating variations for glaciers along highway of Karakoram Mountains.] J. Geogr., 35 (2), 149160. [In Chinese with English summary.]
Xiang-Song, Zhang 1980b. [Recent variations of the Insukati Glacier and adjacent glaciers in the Karakoram Mountains.] J. Glaciol. Geocryol., 2 (3), 1216. [In Chinese with English summary.]
Xiang-Song, Zhang and Desheng, Mi. 1981. [Data of recent change of glaciers in china.] J. Glaciol. Geocryol., 3 (4), 99107. [In Chinese with English summary.]
Zhenshuan, Zhang 1981. [Changes of snowline at the head of Ürümqi river, Tian shan.] J. Glaciol. Geocryal., 3, Special Issue, 106113. [In Chinese with English summary.]


Table. 4 Variations in the frontal positions of Chinese glaciers. Nos 1–14 are glaciers with lengths shorter than or equal to 2km,. Nos 15–51 between 2 and 5 km, Nos 52–96 between 5 and 10 km, and Nos 97–153 longer than 10 km: Jor Nos 154–167 length and/or rate are not clear. “+” sign means advance and “−” sign means retreat