Tarfala Research Station

110 Annual Report 1997–98

Per Klingbjer (Ed.)

Department of Physical Geography Forskningsrapport Research Report No. 110 abcd Tarfala Research Station Annual Report 1997–98

Per Klingbjer (Ed.)

Forskningsrapport 110 Department of Physical Geography Research Report No. 110 abcd Tarfala Research Station Annual Report, 1997-98 Per Klingbjer (ed.) ISSN 1403-9788  The editor and the Department of Physical Geography at Stockhom University Cover figure. Pårteglaciären in Sarek national park (Photo: Per Klingbjer) Printed in Sweden Stockholm, 1999 Högskoletryckeriet, KTH

Mailing adress: Visiting adress: Telephone: Department of Physical geography Svante Arrhenius väg 8 +46 8 162000 Stockholm University Fax: SE-106 91 Stockholm +46 8 164818 SWEDEN Tarfala Research Station Annual Report 1997–98 Contents

Introduction 5

Tarfala Research Station 6

Massbalance of Storglaciären 1997/98 7-10

Mass balance of Mårmaglaciären 1997/98 11-12

Mass balance of Rabots Glaciär, a summary of three years 1995/96, 1996/97 and 1997/98 13-16

Hydrological measurements in the Tarfala drainage basin 1996-98 17-19

Tracer experiment on the water drainage in the accumulation area of Storglaciären 20-22

The mapping of Pårteglaciären and the analysis of its changes from 1963-1996 23-25

Glacio-meteorological investigations on Storglaciären 26

Abstract from the Tarfala student course papers 1998 27-28

Workshop on methods of mass balance measurements and modelling, Tarfala, Sweden. August 10-12, 1998 29-33

Litterature concerning the Tarfala valley and its close surroundings 34-43

Boende på Tarfala forskningsstation under 1998 44-45

Appendix 1. Snow depht survey - May 1998 and winter balance map 1997/98 46

Appendix 2. Stake locations 1998 and summer balance map 1997/98 47

Appendix 3. Stage discharge relationship at Rännan 1986-1997 48

Appendix 4. Stage discharge relationship at Lillsjön 1993-1997 48

Appendix 5. Mean daily discharge at Rännan 1997 49

Appendix 6. Mean daily discharge at Rännan 1998 50 Tarfala Research Station Annual Report 1997–98 Introduction

This year was dominated by the SWEDARP 97/98 the same time data on glacier geology from Scan- expedition, the extensive mass balance programme, dinavia is most useful in interpreting the Antarctic and two conferences to a great extent organised subglacial landscape. by Tarfala staff. It was also the first year when Our experience of the CIRC programme in- MRI-CIRC was fully operational with glacial mete- cludes both positive and negative experiences. The orology, remote sensing and ice coring on the pro- good thing is the potential for future developments gramme. and synergic projects. The rather negative experi- There is a close link between the Antarctic stud- ence was the found that the CIRC programme de- ies and the field work carried out at Tarfala. Meth- veloped in a slight different direction than was ods in mass balance measurements and technical originally planned. The new direction is probably instruments used by us in Antarctica are to a large good for the scientific programme but lead by ne- extent developed and refined at Tarfala. And the cessity to some rather thorough adjustments in the projects associated with Tarfala all benefit from future organisation and use of technical assistance. the support given by the Antarctic programmes. In mid August we hosted a glacier mass bal- Large international programmes like ESF-EPICA ance workshop at Tarfala Research Station. It was and SCAR-ITASE have impacts on glaciology pro- a very successful meeting which will be presented grammes also in northern Sweden. This attracts in the last 1999 issue of Geografiska Annaler. Dur- students and researchers to get involved in glacio- ing the second half of August we organised a IGS- logical tasks, and financial support for investments symposium on the interaction between ice sheets useful also in the north. At the same time the inter- and landscape. The aim of that meeting was to national Antarctic programmes force us to ap- bridge over between theoretical modellers and gla- proach more global problems in our research giv- cial geologists. Though unlucky with the weather ing obvious synergy effects. it was very successful and the proceedings will be The Antarctic programmes are also important published in Annals of Glaciology no. 28. for our studies of past ice sheets over Scandinavia. This year mass balance was measured at 7 glaciers, Radar studies of landforms beneath the present of which 3 are presented in this report. We had one Antarctic Ice Sheet provide us with a unique ana- PhD defence, Jens-Ove Näslund, and one Fil. Lic, logue to former ice age conditions in the past. At Thomas Schneider. It was a very productive year.

May 1998

Per Holmlund Professor

5 Tarfala Research Station Annual Report 1997–98 Tarfala Research Station

Founded 1946

The Field Station

Location: The station is located in the Tarfala Valley, 67°55’N 18°36’E, at 1130ma.s.l. in the Kebnekaise mountains, Swedish Lappland. The valley is surrounded by glaciers and 2000m peaks. Tarfala can be reached by foot (25km hike) or by helicopter from the nearest village, Nikkaluokta. Public transporta- tion is available to Nikkaluokta.

Environment: Arctic alpine environment. The tree line (birch) is at ~700ma.s.l. in the area. Several glaciers in the valley terminate below 1200ma.s.l. Mean annual temperature is –4°C, resulting in wide- spread permafrost conditions.

Availability: The station is open during the summer season: June–September. Summer bookings must be made before May 1. Restricted availability during winter, contact the station director for details.

Station adress: (summer only) Tarfala Research Station c/o Kebnekaise Turiststation S-981 29 Kiruna, Sweden Tel. +46 980 55039 Fax. +46 980 55043

Field Station Management Director: Logistics: Professor Per Holmlund Mats Nilsson Department of Physical Geography Krister Jonsson (until May 31, 1999) Stockholm University Climate Impact Research Centre - Environment S-106 91 Stockholm and Space Research Institute (CIRC - MRI) Sweden Björkplan 6a Tel. +46 8 164811 S-981 42 Kiruna Fax. +46 8 164818 Sweden E-mail. [email protected] Tel. +46 980 826 80 (voice) Fax. +46 980 826 96 (fax) Researcher: Mobile. +46 010 2575272 (Mats) PhD, Research Associate Peter Jansson E-mail. [email protected] Department of Physical Geography Stockholm University S-106 91 Stockholm Sweden Tel. +46 8 164815 Fax. +46 8 164818 E-mail. [email protected]

6 Tarfala Research Station Annual Report 1997–98 Mass Balance of Storglaciären 1997/98

Peter Jansson

Department of Physical Geography, Stockholm University, S-106 91 Stockholm

Abstract. The mass balance record for Storglaciären now comprises 53 years. The winter balance was 1.35 m w.eq., the summer balance was 1.87 m w.eq., yielding a net balance of –0.52 m w.eq. This was the third consecutive year with a negative mass balance. This trend seems consistent with the longer-term cyclicity observable in the mass balance record.

The winter balance was surveyed between April The conversion of snow depths, dsnow, into wa-

24 and May 15, 1998, by Regine Hock (MRI- ter equivalent values , dw.eq, was done by determin- CIRC), Mart Nyman, Constanze Weyhenmeyer ing an empirical relationship between the two. The (University of Bern), Mats Nilsson, Krister Jonsson, data from the density pits and core were plotted as and the author. Snow depth was determined at 287 cumulative water equivalent vs. cumulative snow points by manual probing (Appendix 1). During depth. A second degree polynomial was fit to the the same period, snow density was measured in data (which is nearly linear) yielding dw.eq. = 2 2 four pits at stake locations 5, 10, 15, and 20; stand- 0.00028dsnow + 0.364dsnow - 0.944, R = 1.0. The ard since a few years back. A snow core was also snow depths recorded by probing was then con- extracted from the firn area at stake location 29. verted using this relationship. The resulting grid of The density profiles from these measurements are water equivalent values was then converted into a seen in figures 1–5. Table 1 shows average densi- contour map (Appendix 2) through kriging inter- ties from all measurements. For stake locations see polation using the Golden Software Surfer soft- Appendix 2. At the time of snow density measure- ware. The total accumulation during the winter ments, the snow temperature was well below freez- 1997/98 was 1.35 m w.eq. (figure 6; table 2). ing throughout the snow pack. These conditions During the spring several new ablation stakes prevailed throughout the measurement. were established to improve on the existing abla-

0 0 Stake 5 Stake 10

100 100

200 200

Depth below surface (cm) surface below Depth 300 (cm) surface below Depth 300 0.0 0.2 0.4 0.6 0.0 0.2 0.4 0.6 Density (g/cm 3) Density (g/cm 3)

Figure 1. Snow density at stake location 5, Storglaciären, Figure 2. Snow density at stake location 10, May 1998 Storglaciären, May 1998 7 Tarfala Research Station Annual Report 1997–98

0 0 Stake 15 Stake 20

100 100

200 200

Depth below surface (cm) surface below Depth 300 (cm) surface below Depth 300 0.0 0.2 0.4 0.6 0.0 0.2 0.4 0.6 Density (g/cm 3) Density (g/cm 3)

Figure 3. Snow density at stake location 15, Figure 4. Snow density at stake location 20, Storglaciären, May 1998 Storglaciären, May 1998

0 Table 1. Snow densities at the time of the accumula- tion survey, May 1998 and at the end of the melt Stake 29 season in September 1998. Stake locations are given 100 in Appendix 3.

200 Stake location Snow depth (cm) Density (g/cm3)

300 5 147 0.39 10 125 0.41 15 133.5 0.40 400 20 220 0.42 29 391 0.47

Depth below surface (cm) surface below Depth 500 0.0 0.2 0.4 0.6 Density (g/cm 3) tion gradient I arrive at a summer balance of 1.74 Figure 5. Snow density at stake location 29, m w.eq. for the glacier which is close to the value Storglaciären, May and November 1998 based on spatial distribution of ablation values (1.87 m w.eq.). The balance of the 1998 summer tion stake net. During the winter some stakes were season was 1.87 m w.eq. (Figure 6; table 2). The lost due to accumulation. In September 1998 a to- distribution of melt on the glacier is shown in Ap- tal of 60 stakes (appendix 2) were available for pendix 2. determining the summer balance of the glacier. The The winter and summer balance figures yield a ablation measurements were mainly cared for by net balance volume of –1686 x 103 m3, equivalent Krister Jonsson and Mats Nilsson during the sum- to -0.52 m w.eq., on Storglaciären for the 1997/98 mer. Ablation in areas with no ablation stakes were mass balance year (Figure 7). This was the third extrapolated by using the ablation gradient, calcu- consecutive year with a negative mass balance. The lated from ablation, bs, and elevation values, Z, of trend seems to fit the longer-term cyclic variations the individual stakes in the ablation stake net (Fig- in the mass balance record. ure 7). The ablation gradient from the stake meas- The distribution of winter, summer, and net urements is shown in figure 8 (bs = –0.0043Z + balance with elevation can be seen in figures 9 and 8.0059 m w.eq., R2 = 0.73). Using only the abla- 10.

8 Tarfala Research Station Annual Report 1997–98

3

2

1

0

-1

-2 Balance (m w.eq.) (m Balance

-3

-4 1949/50 1959/60 1969/70 1979/80 1989/90 Mass balance year

Figure 6. The 53 year mass balance record for Storglaciären. Table 2. Mass balance of Storglaciären 1997/98.

Elevation Area Winter balance Summer balance Net balance m a.s.l. 103 m2 103 m3 m w.eq. 103 m3 m w.eq. 103 m3 m w.eq.

1140–1160 3.3 4.5 1.37 12.6 3.82 -8.1 -2.45 1160–1180 7.7 9.5 1.23 29.4 3.82 -19.9 -2.58 1180–1200 17.1 17.7 1.04 61.6 3.60 -43.9 -2.57 1200–1220 35.8 30.8 0.86 115.5 3.23 -84.7 -2.37 1220–1240 53.4 42.9 0.80 152.7 2.86 -109.8 -2.06 1240–1260 63.7 45.8 0.72 164.5 2.58 -118.6 -1.86 1260–1280 83.6 42.8 0.51 209.6 2.51 -166.8 -2.00 1280–1300 80.8 56.8 0.70 201.4 2.49 -144.6 -1.79 1300–1320 95.3 78.3 0.82 233.5 2.45 -155.1 -1.63 1320–1340 149.9 92.4 0.62 333.2 2.22 -240.8 -1.61 1340–1360 271.3 174.7 0.64 570.4 2.10 -395.7 -1.46 1360–1380 320.0 235.1 0.73 645.2 2.02 -410.1 -1.28 1380–1400 254.4 204.2 0.80 502.1 1.97 -297.8 -1.17 1400–1420 118.2 126.6 1.07 220.8 1.87 -94.2 -0.80 1420–1440 78.6 95.2 1.21 142.9 1.82 -47.7 -0.61 1440–1460 66.2 70.8 1.07 114.0 1.72 -43.2 -0.65 1460–1480 82.0 73.4 0.90 133.7 1.63 -60.3 -0.73 1480–1500 149.1 157.5 1.06 226.0 1.52 -68.5 -0.46 1500–1520 228.0 396.7 1.74 355.0 1.56 41.6 0.18 1520–1540 107.6 197.0 1.83 173.8 1.62 23.1 0.21 1540–1560 103.3 180.1 1.74 162.7 1.58 17.4 0.17 1560–1580 101.3 173.7 1.71 154.0 1.52 19.7 0.19 1580–1600 141.8 273.1 1.93 206.9 1.46 66.2 0.47 1600–1620 134.0 291.5 2.18 193.6 1.44 97.9 0.73 1620–1640 162.2 402.6 2.48 232.2 1.43 170.4 1.05 1640–1660 128.5 343.6 2.67 192.3 1.50 151.3 1.18 1660–1680 87.8 237.7 2.71 134.1 1.53 103.5 1.18 1680–1700 61.6 163.1 2.65 95.6 1.55 67.4 1.09 1700–1720 53.4 146.6 2.74 81.9 1.53 64.7 1.21

1140–1720 3239.9 4364.6 1.35 6050.9 1.87 -168.64 -0.52 9 Tarfala Research Station Annual Report 1997–98 Snow depth (cm) 4 0 100 200 300 400 500 O) 2 3 0 R 2 = 0.73 50 2 100 1 150 Ablation (m w.eq.) Ablation 200 0 250 1200 1400 1600 1800 Elevation (m a.s.l.) Water Equvalent (cm H Equvalent Water

Figure 7. Water equivalent values as a function of snow Figure 8. Ablation as a function of elevation (the abla- depth based on density measurements in pits at stake tion gradient) 1998. locations 5, 10, 15, and 20 and core at stake 29 (Fig- ures 1–5).

Net Balance (m w.eq.) 1800

-4 -2 0 2 4 1600 1800 Summer Balance

1600 1400 Winter Balance

1400 (m a.s.l.) Elevation 1200 Net Balance

1200 -4 -2 0 2 4

Elevation (m a.s.l.) (m Elevation Mass balance (m w.eq.)

400 200 0 Figure 10. Winter summer and net balance as a func- tion of altitude, 1997/98. Area (1000 m2)

Figure 9. Net balance and area distribution (%) as a function of elevation, 1997/98.

10 Tarfala Research Station Annual Report 1997–98 Mass Balance of Mårmaglaciären 1997/98

Krister Jonsson

Climate Impacts Research Centre, Environment and Space Research Institute Björkplan 6a, S-98142 Kiruna

Summary winter balance of Mårma amounted to 0.83 m w. eq. (table 1, figure 1). The winter accumulation was determined on April The summer balance was determined in August 18 by Krister Jonsson and Mats Nilsson. The snow 25 by Per Holmlund and Mats Nilsson from four depth probing were performed in 85 points and stake readings and the mapped transient snow line. the snow density was measured in one pit at alti- The ablation gradient was calculated by means of tude 1620 m a.s.l. During that fielwork five abla- linear regression to 0.67 cm/m and was used to tion stakes was put in place on the glacier at alti- calculate the summer balance. The ablation dur- tude 1350, 1400, 1520, 1540 and 1635. An addi- ing the summer amounted to 1.11 m w. eq. (table tional fieldwork by Krister Jonsson and Mats 1, figure 1). Nilsson on May 5 was performed to establish a Thus the net balance was calculated for the gla- new snow density measurement at 1635 m a.s.l cier 1997/98 to –0.28 m w. eq. (figure 1). and complementary snow depth probings in 85 The Equilibrium line altitude (ELA) was calcu- points. The mean density for the snow density pit lated linearly between 1610 and 1630 to 1611 m dugged in May were 0.37 g/cm3. A regression analy- a.s.l. The net balance gradient was determined for sis of the snow density was used to calculate the 1330 to 1635 m a.s.l. to 0.61 cm/m with linear mean snow density at each probing. The mean den- regression (figure 2). The ratio between accumula- sity was then used to convert snow depth meas- tion area and the total area (AAR) was calculated urements to water equivalents (w. eq.). The total to 23%.

1800 bs bn bw

3 3 1700

2 2

1600 1 1

0 0 1500 Elevation a.s.l.) (m -1 -1 Balance (m w.eq.) Balance

1400 -2 -2

-3 -3 1300 1989 1990 1991 1992 1993 1994 1995 1996 1997 1998 1999 -3.00 -2.00 -1.00 0.00 1.00 2.00 3.00 Mass balance year Water equivalent (m)

Figure 1. The mass balance record for Mårmaglaciären Figure 2. Winter (bw), Summer (bs) and net balance (bn) 1989 - 1998. as a function of altitude for Mårmaglaciären 1997/98.

11 Tarfala Research Station Annual Report 1997–98

Table 1. Mass balance of Mårmaglaciären 1997/98.

Elevation Area Winter balance Summer balance Net balance m a.s.l. 103 m2 103 m3 m w.eq. 103 m3 m w.eq. 103 m3 m w.eq.

1320-1340 51.0 31.9 0.63 -108.4 -2.12 -76.5 -1.50 1340-1360 93.0 61.1 0.66 -197.6 -2.12 -136.5 -1.47 1360-1380 151.0 108.1 0.72 -301.9 -1.99 -193.8 -1.28 1380-1400 149.5 103.7 0.69 -280.3 -1.87 -176.6 -1.18 1400-1420 150.5 101.0 0.67 -272.7 -1.81 -171.7 -1.14 1420-1440 161.0 107.1 0.67 -261.6 -1.62 -154.5 -0.95 1440-1460 211.1 131.3 0.62 -343.0 -1.62 -211.7 -1.00 1460-1480 237.5 162.6 0.68 -341.3 -1.44 -178.7 -0.75 1480-1500 193.5 160.1 0.83 -266.0 -1.37 -105.9 -0.55 1500-1520 195.0 174.8 0.89 -243.7 -1.25 -68.9 -0.35 1520-1540 362.0 324.5 0.89 -407.2 -1.12 -82.7 -0.23 1540-1560 359.0 327.2 0.91 -403.9 -1.12 -76.7 -0.21 1560-1580 293.5 229.3 0.78 -256.8 -0.87 -27.5 -0.09 1580-1600 188.0 140.4 0.75 -164.5 -0.87 -24.1 -0.13 1600-1620 334.0 226.4 0.68 -229.5 -0.69 -3.1 -0.01 1620-1640 337.5 258.5 0.75 -210.9 -0.62 47.6 0.14 1640-1660 182.5 191.3 1.05 -102.6 -0.56 88.7 0.48 1660-1680 200.0 252.5 1.26 -75.0 -0.37 177.5 0.89 1680-1700 112.5 149.0 1.32 -42.2 -0.37 106.8 0.95 1700-1720 47.5 65.3 1.37 -5.9 -0.12 59.4 1.25 1720-1740 30.0 41.3 1.37 -3.7 -0.12 37.6 1.25 1740-1760 27.0 37.1 1.37 -3.4 -0.13 33.7 1.25 1760-1780 7.0 9.6 1.37 -0.9 -0.13 8.7 1.24

1320-1780 4073.6 3394.1 0.83 -4523 -1.11 -1128.9 -0.28

12 Tarfala Research Station Annual Report 1997–98 Massbalance of Rabots Glaciär, A summary of three years 1995/96, 1996/97 and 1997/98

Mart Nyman and Truls Neubeck

Department of Physical Geography, Stockholm University, S-106 91 Stockholm

Abstract Here we present the results of mass balance surveys of three consequtive years of Rabots glaciär, Kebnekaise massif. The years 1996, -97and -98 show a net balance of -0.47; -0.14 and –0.47 respectively. The fieldwork has been carried out by various parties from Tarfala Research Station, through the years, not necessarily including the authors at all occations.

Here we present a basic evaluation of three con- In 1998 the winter accumulation (probing by secutive massbalance years of Rabots glacier. Mats Nilsson and Krister Jonsson) amounted to The winter balance survey of 1996, was assisted 0.95 m.w.eq. (table 3) and the summer balance by a visiting group, supervised by Mart Nyman (measured between August 28 and 31, 1998) and Håkan Grudd. This produced a rather dense reached –1.42 m.w.eq. (table 3). Again we see a set of snow survey profiles. The survey was car- net balance of –0.47 m.w.eq. (table 3, figure 1). ried out between May 2 and May 4, 1996. Three The AAR given by field obsevation, is 0.23. density pits were dug at 1130, 1220 and 1380 Comparing results one may note the difference m.s.a.l. respectively. The two first pits, showing in glacier area obtained through planimetry. This shallow snowdepths, yielded mean densitys of 0.33 is probably due to instrumental factors (change of and 0.36 g/cm3. The 1380 m.a.s.l. pit, reaching 300 instrument not corrected for). The net balance, cm, gave a mean density of 0.42 g/cm3. In further however, should be reliable. processing, depths beyond three metres were given a mean density of 0.5 g/cm3, based on the meas- urements in the third pit. The winter accumula- 3 3 tion was measured between May 2 and 4, 1996 and amounted to 1.04 m.w.eq (table 1). Stake read- 2 2 ings in September 7, show an ablation reaching - 1 1 1.51 m.w.eq. (table 1). This gives a net balance of

–0.47 m.w.eq. (table 1, figure 1). The AAR-value 0 0 is estimated to 0.49 by planimetry of field obser- -1 -1 vations made on September 7, 1996. w.eq.) (m Balance The richer winter balance of 1997 was 1.77 m.w.eq. (table 2). Snow probing was performed -2 -2 by Thomas Schneider and Mats Nilsson on May -3 -3 4, 1997. The summer also showed higher ablation 1982 1984 1986 1988 1990 1992 1994 1996 1998 than year the before, with a total meltoff of -2.04 Mass balance year m.w.eq. (table 2). The net balance thus stayed at a Figure 1. The mass balance record for Rabots Glaciär mere -0.14 m.w.eq. (table 2, figure 1). The AAR is 1982 - 1998. in the order of 0.25–0.30 (survey somewhat crip- pled by early snowfall).

13 Tarfala Research Station Annual Report 1997–98

Table 1. Mass balance of Rabots glacier1995/96.

Elevation Area Winter balance Summer balance Net balance m a.s.l. 103 m2 103 m3 m w.eq. 103 m3 m w.eq. 103 m3 m w.eq.

1100-1120 12 3 0.25 33 2.75 -30 -2.50 1120-1140 43 15 0.35 118 2.75 -103 -2.40 1140-1160 67 32 0.48 184 2.75 -152 -2.27 1160-1180 91 44 0.49 250 2.75 -206 -2.26 1180-1200 88 37 0.42 242 2.75 -205 -2.33 1200-1220 127 63 0.49 286 2.25 -223 -1.76 1220-1240 169 107 0.63 380 2.25 -273 -1.62 1240-1260 193 210 1.09 434 2.25 -225 -1.16 1260-1280 220 257 1.17 495 2.25 -238 -1.08 1280-1300 213 150 0.70 480 2.25 -330 -1.55 1300-1320 132 87 0.66 231 1.75 -145 -1.09 1320-1340 140 263 1.88 245 1.75 18 0.13 1340-1360 236 310 1.31 362 1.53 -53 -0.22 1360-1380 271 224 0.83 347 1.28 -123 -0.45 1380-1400 211 174 0.82 267 1.26 -93 -0.44 1400-1420 102 98 0.96 128 1.25 -30 -0.29 1420-1440 103 107 1.04 129 1.25 -22 -0.21 1440-1460 129 123 0.96 161 1.25 -38 -0.29 1460-1480 141 133 0.95 141 1.00 -7 -0.05 1480-1500 183 260 1.42 228 1.25 31 0.17 1500-1520 217 233 1.07 169 0.78 64 0.29 1520-1540 163 136 0.83 133 0.81 3 0.02 1540-1560 103 125 1.21 78 0.75 48 0.46 1560-1580 81 125 1.55 60 0.75 64 0.80 1580-1600 64 107 1.67 48 0.75 59 0.92 1600-1650 113 184 1.63 28 0.25 156 1.38 1650-1700 69 118 1.71 17 0.25 101 1.46 1700-1750 46 102 2.24 11 0.25 91 1.99 1750-1800 17 38 2.25 4 0.25 34 2.00 1800-1850 10 23 2.25 3 0.25 20 2.00 1850-1900 9 20 2.26 2 0.26 18 2.00 1900-1950 5 11 2.26 1 0.26 9 2.00

1100-1950 3767 3917 1.04 5696 1.51 -1779 -0.47

14 Tarfala Research Station Annual Report 1997–98

Table 2. Mass balance of Rabots glacier1996/97.

Elevation Area Winter balance Summer balance Net balance m a.s.l. 103 m2 103 m3 m w.eq. 103 m3 m w.eq. 103 m3 m w.eq.

1100-1120 10 4 0.40 25 2.49 -21 -2.09 1120-1140 31 16 0.51 76 2.45 -60 -1.94 1140-1160 63 45 0.71 152 2.42 -107 -1.71 1160-1180 87 66 0.76 207 2.38 -141 -1.62 1180-1200 84 66 0.78 197 2.35 -132 -1.57 1200-1220 124 105 0.85 287 2.31 -182 -1.46 1220-1240 159 162 1.02 362 2.28 -200 -1.26 1240-1260 190 208 1.09 426 2.24 -218 -1.15 1260-1280 229 284 1.24 506 2.21 -222 -0.97 1280-1300 217 356 1.64 472 2.17 -115 -0.53 1300-1320 133 189 1.42 284 2.14 -95 -0.72 1320-1340 149 196 1.31 313 2.10 -118 -0.79 1340-1360 240 398 1.66 497 2.07 -99 -0.41 1360-1380 271 486 1.79 551 2.03 -65 -0.24 1380-1400 227 427 1.88 454 2.00 -27 -0.12 1400-1420 110 175 1.59 216 1.96 -42 -0.37 1420-1440 116 174 1.50 224 1.93 -50 -0.43 1440-1460 129 204 1.58 244 1.89 -40 -0.31 1460-1480 174 285 1.64 324 1.86 -39 -0.22 1480-1500 199 377 1.90 363 1.83 14 0.07 1500-1520 219 443 2.02 392 1.79 51 0.23 1520-1540 175 412 2.35 307 1.76 104 0.59 1540-1560 103 260 2.54 176 1.72 83 0.82 1560-1580 84 217 2.60 141 1.69 76 0.91 1580-1600 72 191 2.65 119 1.65 72 1.00 1600-1650 123 338 2.75 196 1.59 143 1.16 1650-1700 71 195 2.75 107 1.50 88 1.25 1700-1750 48 132 2.75 68 1.42 64 1.33 1750-1800 19 51 2.75 25 1.33 26 1.42 1800-1850 11 30 2.75 14 1.24 17 1.51 1850-1900 10 28 2.75 12 1.16 16 1.59 1900-1950 6 17 2.75 6 1.07 10 1.68

1100-1950 3881 6535 1.77 8408 2.04 -1207 -0.14

15 Tarfala Research Station Annual Report 1997–98

Table 3. Mass balance of Rabots glacier1997/98.

Elevation Area Winter balance Summer balance Net balance m a.s.l. 103 m2 103 m3 m w.eq. 103 m3 m w.eq. 103 m3 m w.eq.

1100-1120 16 4 0.25 44 2.73 -40 -2.48 1120-1140 35 12 0.35 93 2.65 -80 -2.30 1140-1160 73 33 0.46 187 2.56 -154 -2.11 1160-1180 83 38 0.46 206 2.48 -168 -2.02 1180-1200 94 44 0.47 226 2.40 -182 -1.93 1200-1220 123 64 0.52 285 2.32 -221 -1.80 1220-1240 169 109 0.64 378 2.24 -269 -1.59 1240-1260 207 155 0.75 446 2.15 -291 -1.41 1260-1280 226 175 0.77 468 2.07 -294 -1.30 1280-1300 262 209 0.80 522 1.99 -313 -1.19 1300-1320 129 106 0.82 246 1.91 -140 -1.09 1320-1340 135 110 0.81 247 1.83 -137 -1.01 1340-1360 252 229 0.91 440 1.74 -211 -0.84 1360-1380 271 275 1.02 451 1.66 -175 -0.65 1380-1400 221 244 1.10 349 1.58 -106 -0.48 1400-1420 109 112 1.03 163 1.50 -51 -0.47 1420-1440 122 129 1.05 173 1.42 -44 -0.36 1440-1460 156 162 1.04 208 1.33 -47 -0.30 1460-1480 159 171 1.08 199 1.25 -28 -0.18 1480-1500 200 246 1.23 234 1.17 12 0.06 1500-1520 211 264 1.25 230 1.09 34 0.16 1520-1540 168 210 1.25 169 1.01 41 0.24 1540-1560 106 133 1.25 98 0.92 35 0.33 1560-1580 89 111 1.25 75 0.84 36 0.41 1580-1600 77 96 1.25 59 0.76 38 0.49 1600-1650 141 176 1.25 87 0.62 89 0.63 1650-1700 81 101 1.25 33 0.41 68 0.84 1700-1750 55 69 1.25 11 0.21 57 1.04 1750-1800 23 29 1.25 3 0.15 25 1.10 1800-1850 11 14 1.25 2 0.15 12 1.10 1850-1900 10 13 1.25 2 0.15 11 1.10 1900-1950 6 8 1.25 1 0.15 7 1.10

1100-1950 4020 3848 0.95 6334 1.42 -2486 -0.47

16 Tarfala Research Station Annual Report 1997–98 Hydrological measurements in the Tarfala drainage basin 1996-98

Thomas Schneider

Department of Physical Geography, Stockholm University, S-106 91 Stockholm

Abstract Discharge rating curves were established for Rännan and Lillsjön gauging stations in the Tarfala drainage basin. The measurements showed a stable relationship between stage and discharge at both stations. At Lillsjön more measurements above 4 m3s-1 are needed to con- solidate the rating curve.

Introduction Discharge variations Water discharge measurements in the Tarfala drain- Discharge in Tarfala started around the end of June age basin were carried out at the gauge stations at (Figure 3, 4). In the beginning of the melt season Lillsjön and Rännan as part of the measuring pro- water levels at the gauge stations often are overes- gram of the research station. In addition, during timated due to damming of snow and ice in the summer 1998 discharge was measured at Nordjåkk flume and the outlet of Lillsjön. The peak around and Sydjåkk, the proglacial streams draining June 22, 1997 and June 25, 1998 is therefore prob- Storglaciären (Frödin and Schneider, 1999). ably not a true discharge peak. Discharge in 1997 3 -1 Methods was characterised by low peaks (~ 8 m s , Appen- dix 5) and a quite constant mean monthly discharge Water level were measured at the gauge stations (Table 1). The hydrograph was mainly dominated using pressure transducers and Campbell Scientific by diurnal variations due to the influence of high dataloggers. The stage-discharge relationship at Rännan was established by discharge measure- ments using the salt dilution method with instan- 2.0 taneous injection (Schneider, 1998). At Lillsjön dis- charge was measured with a current meter. At Q = 3.4845 h 3.0368 Rännan air temparature and precipitationn is meas- 1.5 ured using a Pt100 and a tipping bucket, respec- tively. In 1998 the tipping bucket failed.

(m) 1.0 1986 Rating curves h 1993 1996 The rating curve for Rännan was determined from 1997 0.5 measurements from 1986 to 1997 (Figure 1, Ap- pendix 3). We found that the rating curve was rela- tively stable even though there was an avalanche 0.0 which destroyed parts of the flume in 1991. Meas- 0 5 10 15 20 urements continued in 1992 and the flume was 3 -1 totally rebuilt in 1996. At Lillsjön no discharge Q (m s ) 3 -1 measurements could be carried out above 4 m s Figure 1. Discharge rating curve Rännan. h is water stage due to limitations of the current meter. The rating in the flume with a zero level at the lowest point of the curve was calculated from measurements in 1993 flume at the inlet into the tube. Q is discharge. The rat- and 1995-1997 (Figure 2, Appendix 4). ing curve was fitted by regression analysis.

17 Tarfala Research Station Annual Report 1997–98

0.6 melt rates. The summer of 1997 was unusual dry and warm. Discharge peaks in 1998 were more distinct with a maximum daily discharge of 19.5 1993 0.5 m3s-1 on July 13 (Appendix 6). Mean summer dis- 1995 1996 charge was slightly higher in 1998 but monthly 0.4 1997 variations were larger (Table 1).

Table 1. Mean monthly discharge at Rännan in 1997 (m) 0.3

h and 1998. June July Aug Sept Mean 0.2 1997 1.946 4.254 3.909 2.530 3.160 1998 1.800 7.153 3.856 1.842 3.662 Q = 9.1916 h 1.2004 0.1 R 2 = 0.97 Conclusions 0.0 012345The discharge measurements from Rännan showed 3 -1 that the flume is quite stable over the years. No Q (m s ) significant change due to the avalanche could be Figure 2. Discharge rating curve at Lillsjön. h is water stage in the tube. The zero level is defined by a staff found. The problem of extrapolating the rating gauge. Q is discharge. The rating curve was fitted by curve to high discharge at Lillsjön still exists where regression analysis. no calibration measurements exist.

) 6 -1

3

P (mmd 0 20

10

0 12 T (°C) -10

) 8 Rännan -1 -20

s Lillsjön 3

Q (m 4

0

1-jun 21-jun 11-jul 31-jul 20-aug 9-sep 29-sep 19-okt

Figure 3. Discharge, air temperature and precipitation at Rännan and discharge at Lillsjön in 1997. The discharge peak in the beginning of the melt season is probably due to overestimating water stage due to ice damming in the flume.

18 Tarfala Research Station Annual Report 1997–98

20

10

0 T (°C) -10 16 -20

12 ) Rännan -1

s Lillsjön 3 8 Q (m

4

0

27-maj 16-jun 6-jul 26-jul 15-aug 4-sep 24-sep 14-okt

Figure 4. Discharge and air temperature at Rännan and discharge at Lillsjön in 1998. The discharge peak in the beginning of the melt season is probably due to overestimating water stage due to ice damming in the flume.

References Station Annual Report 1997-98. Department of Physical Geography, Stockholm University, Research Bronge, C., 1989: Climatic aspects of hydrology and Report 109: 20-22. lake sediments with examples from northern Sweden Schneider, T. 1998: Hydrological measurements in the and Antarctica. Department of Physical Geography, Tarfala drainage basin 1995/96. In: Klingbjer, P. (ed.): Stockholm University, Meddelande nr A241. 166p. Tarfala Research Station Annual Report 1996–97. Frödin, S. and Schneider, T., 1999: Tracer experiment Stockholm University, Department of Physical on the water drainage in the accumulation area of Geography, Research Report 105: 26-28. Storglaciären. In: Klingbjer, P. (ed.): Tarfala Research

19 Tarfala Research Station Annual Report 1997–98 Tracer experiment on the water drainage in the accumulation area of Storglaciären

Sara Frödin and Thomas Schneider

Department of Physical Geography, Stockholm University, S-106 91 Stockholm

Abstract During the melt season 1998 a dye tracer experiment was conducted in the upper part of the accumulation area of Storglaciären. On 28 July the fluorescent dyes Rhodamine B and Fluoresceine were spread out on the snow surface and injected into the firn aquifer at a depth of 15 m, respectively. Watersamples were collected in the proglacial streams, Nord- and Sydjåkk, throughout the ablation season. The maximum flow velocities were calculated to 13 mh-1 for Rhodamine and 40 mh-1 for Fluoresceine indicating a well-developed englacial drainage system in the firn area. From the time lag between first emergence of Fluoreceine and Rhodamine percolation velocity through the firn layer was estimated to 0.1 mh-1. The cumulative tracer return was 5% for Rhodamine B and 53% for Fluoresceine. The dyes appeared only in Nordjåkk, which indicates a divided englacial drainage system.

Introduction time and flow velocity were calculated. The time lag between the first emergence of Fluoresceine and The firn layer in the accumulation area of temper- Rhodamine gave an estimate of maximal percola- ate glaciers plays an important role for the delay tion velocity through the unsaturated part of the of run-off from glacierised drainage basins. Melt- firn layer. water percolates through the firn and a water-satu- rated layer is formed above the firn-ice transition Discharge (Schneider, in press). To investigate the connection Discharge measurements were made in Nord- and between the drainage system in the accumulation Sydjåkk to establish new rating curves (Figure 2) and ablation area, and estimate the travel time and and to compute recovery curves for both tracers flow pathways of meltwater from the firn surface (Figure 3). A total of 26 salt dilution tests were to the terminus of the glacier, a tracer experiment done in Nordjåkk and 17 in Sydjåkk with a self- was carried out in the accumulation area of integrating instrument (Schäppi AF93) in order to Storglaciären. determine the stage-discharge relationship. Water stage was recorded in both streams during the pe- Methods riod 15 July-10 September, with Geokon 4500 ALV Dye tracer test vibrating wire pressure transducer connected to Two fluorescent dyes - Rhodamine B and Fluore- CR10 Campbell datalogger. The stage readings sceine - were injected in the firn area about 100 m were transformed to discharge values with the help downglacier of Svartaväggen (Figure1). Rhoda- of the rating curves (Figure 2). mine B (12kg) was spread out on the snow sur- Results and discussion face, covering an area of 4×4 meters, and Fluore- Fluoresceine was first detected in Nordjåkk 74 h sceine (5kg) was injected into the firn aquifer after injection and Rhodamine B 231 h after in- through a borehole at 15 meters depth. Water sam- jection. With a linear distance of 3 km maximum ples were thereafter collected in the proglacial velocity was estimated to 41 mh-1 and 13 mh-1, re- streams with ISCO automatic samplers at inter- spectively. Hooke et al. (1988) injected dye into a vals of 1-3 hours throughout the ablation season. borehole just below the equilibrium line 400 m The water samples were later analyzed with a below the dye injection site. They calculated a Perkin Elmer LS 50 B spectral fluorometer to de- maximum flow velocity through the englacial termine dye concentration. From these data travel

20 Tarfala Research Station Annual Report 1997–98

Dye injection

Nordjåkk

Sydjåkk

Figure 1. Location map of Storglaciären. drainage system of 72 mh-1. Applying this velocity drainage system in the accumulation area. The time on the dye injection site the travel time from there lag between first emergence of Fluoresceine and to the terminus of the glacier would have been 43 Rhodamine at Nordjåkk (157 h) was due to per- hours. This results in a residence time of the water colation through the firn layer. With a percolation in the firn aquifer of ~30 h. Schneider in press cal- depth of 15 m a maximum percolation velocity was culated average linear velocity in the firn aquifer estimated to 0.1 mh-1. This is in good agreement on Storglaciären to be 0.12 mh-1. With the above with a mean percolation velocity of 0.25 mh-1 cal- residence time the dye should have reached the culated by Schneider in press at the same site. englacial drainage system ~3.6 m from the injec- No tracer appeared in Sydjåkk indicating that tion site. This indicates a well-developed englacial most of the water from the accumulation area is drained by Nordjåkk, in accordance with earlier 1.5 studies (Stenborg, 1969, Hooke et al. 1988). Cumulative tracer return in Nordjåkk was 5%

4.2393 for Rhodamine B and 53% for Fluoresceine. Most Qsydjokk = 0.68972×s of the Rhodamine probably was retained in the unsaturated part of the porous firn layer. 1.0 Conclusions The dye tracer test in the accumulation area of

Stage (m) Stage Storglaciären yielded a maximum travel time of 9 (2.5335 × s) 0.5 Qnordjokk = e × 0.11627 days from the surface to the terminus of the gla- cier. Dye injected into the firn aquifer reached the terminus within 3 days which was explained by a well-developed englacial drainage system near the 0.0 injection hole. The time lag between the two trac- 0.0 1.0 2.0 ers gave a percolation velocity through the unsatu- -1 Discharge (m³/s) rated part of the firn layer of 0.1 mh . All dye ap- peared only at Nordjåkk indicating a division of the drainage system of Storglaciären. Figure 2. Stage-discharge relationship at Nordjåkk and Sydjåkk, 1998.

21 Tarfala Research Station Annual Report 1997–98

) 1.2 -1

s 0.9 Nordjåkk 3 0.6 0.3 Q (m Sydjåkk ) ) 3 0.9 1 -1 -1

Fluoresceine 0.8 n

2 0.6 r

0.6 u Rhodamine t e r

0.4 e 1 0.3 y D 0.2

Fluoresceine flux (mg s flux (mg Fluoresceine 0 0 0 Rhodamine B flux (mg s (mg flux B Rhodamine 30-jul 4-aug 9-aug 14-aug 19-aug 24-aug 29-aug 3-sep 8-sep 13-sep

Figure 3. Dye flux curves, tracer return and discharge at Nordjåkk and Sydjåkk

References Schneider, T., in press: Water movement in the firn of Storglaciären. Journal of Glaciology. Hooke, R.LeB., Miller, S.B. and Kohler, J., 1988: Char- Stenborg, T., 1969: Studies of the internal drainage of acter of the englacial and subglacial drainage sys- glaciers. Geografiska Annaler. 51 A (1-2): 13-41. tem in the upper part of the ablation area of Stor- glaciären, Sweden. Journal of Glaciology 34(117): 228-231.

22 Tarfala Research Station Annual Report 1997–98

The Mapping of Pårteglaciären and the Analysis of its Changes From 1963-1996

Frank Neidhart

Department of Geodesy and Geomatics Engineering, University of New Brunswick P.O. Box 4400, Fredericton, NB, CANADA E3B 5A3

Introduction lation. The other part of the fieldwork was to pho- tograph the glacier with a calibrated “Rolleiflex The Pårteglaciären is located in Northern Sweden 6006 metric“ camera, with focal lengths of 50 mm, at 67°09’ N and 17°51’ E. Its ice sheet reaches from 80 mm and 150 mm, respectively. These photo- about 1080 m MSL to a maximum height of about graphs were taken from the surrounding ridges on 1800 m MSL with an extension of maximum 4.5 the north and south sides of the glacier. Priority times 5.2 km (=10.6 km²). The objectives of the was given to the front area of Pårteglaciären, but project were: (1) To map the glacier including the approximately 60 additional photographs (over- surrounding area of 93 km2 using the latest black- lapping and convergent) with different camera con- and-white photographs, (2) To generate Digital stants covered the rest of the ice. Terrain Models (DTM) for the years 1963, 1980 and 1992, and (3) To calculate the area- and vol- Aerotriangulation and data collection ume-changes, and the front-retreat for the above In order to achieve maximum accuracy when deal- years. Three sets of photographs were available. ing with aerial photography, single images or stereo Photographs 63 Hf 274 11-19, taken in 1963, and models have to be combined to a single block, in 92826 1–5, taken at September 12, 1992. Both sets order to bridge areas or models without any ground were in black-and-white at an approximate scale control points. With sufficient ground control, of 1:30000, taken by the Swedish Landsurveying nearly the same accuracy as in a single model can Administration, LMV. Furthermore, a set of four be achieved. In this work, the bundle adjustment infrared photographs at 1:60000, photos IRF program PATB-GPS was used. The newest set of 288009-288011. photographs was used for the aerotriangulation and Fieldwork it was proven that the GPS survey and the drilled points fit together. The adjusted coordinates of Photogrammetric ground control was provided by 1992 were then taken to absolutely orient the other points, drilled into the photographic emulsion. image sets in order to have the same vertical da- However, due to large discrepancies between the tum for the analysis. adjusted heights of the drilled points by means of In order to produce a Digital Elevation Model aerotriangulation, and the corresponding heights (DEM) or a Digital Terrain Model (DTM), which in the topographic map (1:100000, Sarek National- will then be the base for the following steps of park, BD10), it was decided to perform a field sur- analysis and topographic mapping, the surface of vey by means of GPS and establish new ground the entire area has to be represented as well as pos- control to confirm or disprove the given coordi- sible. Various methods of data collection are nates of the drilled points. Therefore, five new known, such as measurements of a Triangular Ir- ground control points on well identifiable rocks regular Network (TIN), direct measurement of were measured in the vicinity of the corners of the constant height intervals, profiles, or a regularly strip of photographs of 1992 for integration with spaced raster. The most common approach in ana- the drilled points into one combined aero-triangu-

23 Tarfala Research Station Annual Report 1997–98 lytical photogrammetry is a regularly spaced grid Visualization and analysis of the DTMs in combination with break- and formlines, i.e., SCOP offers a wide spectrum of possibilities for abrupt and smooth changes in slopes, respectively. the visualization and analysis of a DTM. Contour The regular spacing should be chosen as 2-6 mm lines at 10-m-intervals in DXF were produced for in the map, i.e., for the planned map-scale of the mapping of the glacier. Furthermore, five 1:20000, 40-120 m (Ackermann 1994). In order longitudinal profiles, pixel maps and perspective to preserve as much detail as possible, a 40-m-grid views for a 3-dimensional visualization of the DTM in combination with break lines was measured for were created. Finally, always two DTMs at a time all permanently snow- and ice covered areas. In were intersected to create a so-called differential this step, also other problem areas, such as very model, that is, to create a new DTM consisting of steep slopes or regions in shadow areas, where the the height differences between two corresponding light-conditions were very diffuse, were sampled. points of each input DTM to calculate the volume This was done for all three sets from 1963, 1980 change. and 1992. The second step of data collection was Generation of a digital orthophoto map done automatically using PHODIS® ST, the photogrammetric software by Zeiss. It was carried A digital orthophoto contains all the details of an out for the reminder of the area, mainly open fields, area given in the original photograph in a given which was just used for mapping purposes. The scale, and no information is lost due to images of set 92 were scanned using the Zeiss generalization. Every point or feature is shown at photogrammetric precision scanner SCAI with a its true position, which makes it therefore more resolution of 14 mmm (about 1820 dpi). The ad- suitable for interpretation and information vantage of automatic DTM generation is the prin- gathering. From a photogrammetric point of view, ciple of redundancy. The idea is, to sample up to a digital orthophoto can easily be generated if the 100 times more points than what is usually done scanned images, including their interior and analytically, in order to get a high accuracy DTM. exterior orientations, as well as a DTM are It is common practice (e.g. Ackermann 1994, available. With the use of PHODIS® OP, the Zhang and Miller 1997), to sample points every orthophoto module from Zeiss, two digital 10-15 pixels in the digital image, hence, at an im- orthophotos were produced at scales of 1:15000 age scale of 1:30000 and 14 mm resolution, at 4.2 and 1:20000, with corresponding ground m to 6.3 m. In this case, a slightly coarser resolu- resolution of 1.5 m and 2.0 m, respectively. tion of 7.5 m was selected. Analysis and results DTM generation The (horizontal) areas of Pårteglaciären and SCOP is a very sophisticated and powerful DTM Palkatjekna (table 1) were directly calculated using software package (Sigle et. al 1991), where nearly the polygons sampled as breaklines during the every step can be controlled by the user. SCOP uses DTM data collection. These surroundings consisted the bell-curve as basic algorithm, i.e. the DTM is of a large number of points for each glacier, smoother than when using linear interpolation representing the glacier sufficiently. However, it is methods, because the scatter of the individual obvious that the glacier seemed to have grown in points is suppressed. Two DTMs of the set 92 were between 1980 and 1992 (table 1), although there generated, one with a 15 m spaced regular grid for Table 1. Change of the areas the purpose of the following analysis and one with a 40 m regular grid, which is better for other users due to the smaller file size. Furthermore, two DTMs Year Pårteglaciären Palkatjekna for the years 1980 and 1963 were generated. The input files were enlarged by an additional surrounding belt of raw data from set 92 (all Absolute areas (km2) bedrock, where no changes were expected in this 1963 - 1980 11.420 - 10.611 2.890 - 2.562 29-year-period). The reasons for this step were 1980 - 1992 10.611 - 10.622 2.562 - 2.626 twofold: firstly, due to the used algorithm, the raw DTM data should not end directly at the glacier’s Actual change (m2) edge, and secondly, a 500-m-belt gives a pleasant 1963 - 1980 -505580 -208261 view of the area for the resulting topographic maps 1980 - 1992 -218240 -101644 of set 63 and set 80, respectively.

24 Tarfala Research Station Annual Report 1997–98

6 3 was a large front-retreat (table 2). This was Table 3. Volume change (10 m ) with absolute probably due to the fact that there was more snow accuracy in the accumulation areas in 1992, therefore, the front-areas were compared separately for the analysis (Jansson personal communication). Finally, Year Pårteglaciären Palkatjekna the middle-moraines were used to divide the glacier into five accumulation areas with corresponding 1963 - 1980 -139.9 (±7,67%) -19.8 (±13,75%) areas of 27.47 %, 25.17%, 27.57%, 8.64%, and 1980 - 1992 -54.5 (±18,32%) -9.8 (±25,32%) 11.13% of the entire area from north towards south, respectively. The same polygons were used to determine the Finally, the important spot-heights were sam- front retreat (table 2). This was measured in the pled during the data-collection for the morphol- direction of the estimated ice-flow, in small, parallel ogy. All heights from the topographic map BD10 lines. The differences from 1992 to 1996 were were re-measured, and also some additional heights computed by the difference between the 1992- for lakes and peaks were collected. The accuracy polygon and a delineation of the front area of 1996 of the new heights corresponds to the standard using the new images obtained in the field survey, deviation of single points as obtained from the oriented with natural features coordinated in the absolute orientation (about 0.5 m). The differences 1992 images. in single spot heights were up to 15 m.

Table 2. Frontretreat(m) for Pårteglaciären The mapping using MicroStation The last step of the project was the cartographic mapping of the entire area with the CAD program Year Minimum Maximum Mean MicroStation. Guidelines for the map design were older maps from Mikkaglaciären and the Tarfala- 1963 - 1980 128 329 204 area. All features, except for the crevasses, were 1980 - 1992 37 179 118 taken from set 92. The crevasses were taken from 1992 - 1996 11.5 81.5 45 set 80, since they were not visible in set 92 due to snow. The result were maps in 1:15000 and 1:20000, with the former restricted to the glacier Due to the interpolation method (bell curve) areas. Furthermore, two simple line maps of the used by the DTM-software SCOP (ver. 3.3.1), it years 1963 and 1980 were produced by simply can be stated that the accuracy of the entire DTM importing the DXF-break lines and 10-m-contour σ intervals from SCOP into MicroStation and print- DTM is higher than the accuracy of a single point σ ing at a scale of 1:15000. h. This is due to the fact that the scatter of the measured points is suppressed by the program and References the DTM is smoothed. On a smooth, rolling sur- Ackermann, F., 1994. Digital Elevation Models- face like this glacier, the DTM should therefore have Techniques, and Application, Quality Standards, a very high vertical accuracy. The estimation of Development. Proceedings: Symposium on Mapping the accuracy in volume change (table 3) is there- and Geographic Information Systems, ISPRS, Vol. fore overcautiously done by multiplying the gla- 30(4), pp. 421-432 cier-surface of the larger ice area of the correspond- Sigle, M., Hellwich, O. and Köstli, A.. 1991, Intersection and Combination of Digital elevation Models - ing sets, with the accuracy of a single point meas- Methods and Applications, White Paper - INPHO urement gained in the process of absolute orienta- GmbH, Stuttgart tion of both years and applying error propagation. Zhang, Bingcai. and Miller, Scott. 1997. Adaptive Hence, the relatively large standard deviation re- Automatic Terrain Extraction, Proceedings of SPIE, sults from the fact that the considered uncertainty Vol. 3072, Integrating Photogrammetric Techniques with Scene Analysis and Machine Vision, pp 27-36. is relatively high compared to the melted down amount. However, it has to be pointed out again that the real accuracy can be seen as being better than the absolute accuracy.

25 Tarfala Research Station Annual Report 1997–98 Glacio-meteorological investigations on Storglaciären

Regine Hock

Climate Impacts Research Centre, Environment and Space Research Institute Björkplan 6a, S-98142 Kiruna

Abstract An automatic weather station was operated on Storglaciären during the melt season 1998. The data will be used to develop and improve existing models to compute glacier melt and discharge on an hourly time scale using both energy balance and temperature index methods. Energy partioning and cumulative melt will also be related to the synoptic weather patterns.

Measurements sensitivity and the effect of climate scenarios on computed melt are envisaged. From mid June to mid September an automatic 2. Emphasis is placed on the parameterization of weather station was operated close to the equilib- grid-based computation of the radiative energy rium line on Storglaciären. Hourly data of air tem- fluxes in steeply sided terrain. In particular the perature, relative humidity (at 1 and 2 m), wind parameterization of longwave incoming radiation speed (at 1 and 2 m), wind direction, global radia- using cloud cover data or merely global radiation tion, reflected short-wave radiation, longwave in- data will be focussed on. coming and outgoing radiation, surface lowering, 3. The relative contribution of the energy fluxes ice temperatures (down to 33 m below the surface) to melt and cumulative melt will be related to the and precipitation were collected. In September 5 synoptic weather context, thus moving from an thermistors were installed at different heights above hourly time scale to a time scale of a few days or the ice surface to monitor snow temperatures dur- weeks and also linking the point-scale measure- ing coming winter accumulation. The weather sta- ments to larger-scale atmospheric conditions. The tion will be installed for a second melt season in resarch will focus on these links and their poten- 1999. tial for operational use in melt forecasting. Purpose References These data will be used for several purposes: Hock, R., 1998. Modelling of glacier melt and discharge. 1. Existing melt models computing glacier melt Zurcher Geographische Schriften 70, Department of and discharge on an hourly basis (Hock, 1998) will Geography, ETH Zurich. 140 p. be tested and improved. The assessment of their

26 Tarfala Research Station Annual Report 1997–98 Abstracts from the Tarfala student course papers 1998

Abstracts compiled and edited by Jens-Ove Näslund

Department of Physical Geography, Stockholm University, S-106 91 Stockholm

The following abstracts describe the seven student projects that were conducted during the 1998 field course in glaciology at Tarfala research station. The course has been given for undergraduate student each year since the late 1950’s, and includes both a theoretical part with lectures and individual fieldworks resulting in written reports. The reports are in Swedish. Persons interested in the contents of these student reports may contact Jens-Ove Näslund.

Calculated ablation from climate data Storglaciären and Isfallsglaciären. The subglacial compared to measured ablation morphology of the eastern side of the Kebnekaise massif is caused by preferential erosion by ice mov- Ulf Jonsell and Inger Jöborn ing perpendicular to the dip of different bedrock Estimation of ablation is of great interest in stud- units. Overdeepenings are formed where the bed- ies of climate change, energy supply and much rock is more easily eroded. more. In this paper a comparison has been made between calculated (data from a meteorological Isfallsglaciären - frontal position and ice station on the glacier) and actual ablation(data velocity through a cross-section from measured ablation stakes) at Storglaciären, Sweden. The fluxes of energy have been calculated Hanna Skarelius and Karin Willis by the method of energy balance. Two methods The ice flux through a transverse profile of were used to get the netradiation: 1) Parameter- Isfallsglaciären has increased with 20% and the ization of long wave incoming radiation based on ice velocity along a cross-section has increased observation of clouds and 2) from a netradiation about 10 m/a since last year (1997). The northern instrument. The calculated values of ablation were part of the front of Isfallsglaciären is advancing. on average 22% (method 1) and 44% (method 2) There is a long tradition of glacial-climatological lower than the measured values. The underestima- studies in northern Scandinavia. The state of gla- tion is probably due to fog and precipitation dur- ciers vary due to fluctuations in climate, especially ing the survey. This has been observed also in pre- regarding precipitation and temperature. Isfalls- vious studies. glaciären in the Kebnekaise massif is an example of a glacier that has been investigated for this pur- Overdeepenings in the Kebnekaise massif pose. The aim of the present study was to compare ice fluxes and ice velocities at Isfallsglaciären be- Anna Engström and Nicholas Hall tween 1997 and 1998, and to study changes in the Radio-echo soundings of Kebnepakteglaciären at position of the front over the period 1959 to 1998. Kebnekaise, northern Sweden, show that there is In addition to a discussion on the climatic influ- an overdeepening in the bed topography of the ence on the movement of the glacier, the impor- glacier. The overdeepening is located in the same tance of the underlying topography and ice thick- striking direction as the overdeepenings beneath ness is discussed.

27 Tarfala Research Station Annual Report 1997–98

The Kebnepakteglacier 1998 - mass balance Profile measurements of Storglaciären made and the location and topography of the with GPS - a comparison with previous glacier snout optical measurements Mattias Lindén and Toomas Randsalu Peter Olsson and Johan Sandell

The front of Kebnepakteglaciären, northern Storglaciären in northern Sweden is a valley glacier Sweden, is expanding into the Tarfala lake. Our with a divided accumulation area and a smooth investigation indicate that Kebnepakteglaciären has longitudinal profile. The massbalance of advanced ~18 m since 1990. The calculated mass- Storglaciären well represents the conditions at other balance for 1998 is close to steady-state to slightly glaciers in the Kebnekaise area. Measurements of positive. Also eyewitness data show that the glacier the ice surface topography gives good information has advanced during the 1990’s. The results of the on how the glacier mass balance is changing. The present study contain several uncertain factors due glacier mass balance provides filtered and delayed to approximations in the basis for the different cal- information of the climate. The results show that culations. Two of the main problems were a failure the longitudinal surface profiles of Storglaciären of radarmeasurements and uncertainties regarding indicate a reduced thinning rate. Some of the trans- the ablation area. The problems with the radar verse profiles even show an increase in ice thickness. equipment resulted in only one measured depth in The results probably reflect increased precipitation the investigated cross-section, which gave large un- and lowered summer air temperatures. The profile certainties in the model of the of the cross-section measurements were made with differential GPS area. The area of the ablation zone was roughly with an vertical accuracy of a few cm. The process- estimated during fieldwork. Finally, ablation values ing of the GPS data showed that the technique of from Storglaciären were used to calculate the ab- using differential GPS for surface profiling on lation for Kebnepakteglaciären. Storglaciären is applicable and can produce very good results, also close to the steep valley walls beside the glacier. Crystallographic studies of moraine features on the snout of Storglaciären Changes in water discharge with air Anna Berntsson and Helena Westin temperature The debris-bands that are situated on the front of Tanja Johansson and Magdalena Sandberg Storglaciären, northern Sweden, show signs of plastic deformation, according to Hooke’s model An analysis of the correlation between air tempera- of glacier flow. Ice samples were collected from ture above Storglaciären, northern Sweden, and the different locations along a profile perpendicular to discharge of Nordjåkk and Sydjåkk in front of the the debris-band. The crystals show no elongated glacier has been made. Weather conditions during forms detectable in polarized light.However, the the field period made it difficult to draw any defi- ice contained airbubbles with a strong preferred nite conclusions from temperature only. Clouds and orientation; the same orientation as the debris- precipitation had a significant impact on the re- bands and other structures in the ice. This indicates sults. However, the results indicate a time lag be- that plastic deformation has taken place. The two tween temperature rise and the following discharge largest debris-bands are dipping 62° towards west. peak for Sydjåkk, while for Nordjåkk the tempera- The debris-bands reached the surface of ture rise and discharge peak was simultaneous. This Storglaciären in summer 1994. As a result of differ- can be explained by different drainage paths ential ablation, ice-cored moraine ridges have through the glacier for the two streams. There is a formed. daily variation in discharge that can not be seen in either temperature or precipitation. The daily vari- ation might be caused by solar radiation.

28 Tarfala Research Station Annual Report 1997–98 Workshop on Methods of Mass Balance Measurements and Modelling, Tarfala, Sweden August 10-12, 1998

Andrew Fountain

Department of Geology, Portland State University, Portland, OR 97207-0751, USA

Peter Jansson

Department of Physical Geography, Stockholm University, S-106 91 Stockholm, Sweden

Abstract A three-day workshop was held at the Stockholm University research station at Tarfala, northern Sweden. The workshop was organised in response to current interest in mass bal- ance data for assessing the effect of climatic variations and to the increasingly tight financial limitations imposed on mass balance programs. Given these conditions, time was ripe to re- examine our methodologies towards producing an increasingly accurate data set using the most cost-effective methods. In addition, we wanted to highlight approaches to difficult but typical situations, such as debris-covered, highly-crevassed, or extremely large glaciers; and to examine new technologies such as remote sensing.

Introduction the basis for many of the mass balance programs in existence today, including the U.S. and Canada. Recent symposia and workshops on glacier mass In the 34 years since the IHD, much experience balance programs have focused on implications of has been gained although there has been little op- climate change. Some of these include, Symposium portunity to exchange this information in an effi- on Glacier Fluctuations and Climatic Change, cient manner. Moreover, rapid technological de- Amsterdam, 1987 (Oerlemans 1989); Symposium velopments, including both instrumental and com- on Ice and Climate, Seattle, 1989 (IGS 1990); Sym- putational, present new techniques to assess gla- posium on Glacier Mass Balances, Innsbruck, 1994 cier mass change. (ZGG 1997); Antarctica and Global Change, Ho- bart, 1997 (IGS 1998). Others have focused on Scope of the workshop water resources and hydrology (Northern Hydrol- Glacier mass balance data has gained increased at- ogy Symposium, Saskatoon, 1990; International tention because of its importance in detecting glo- Workshop on Glacier Hydrology, Cambridge, bal climate change and its influence on global sea 1993). The last meeting on methodology was held levels, in addition to its importance to regional wa- in 1962, “Problems of Mass Balance Studies“ in ter supplies and power generation. This resurgence Cambridge, England (IGS 1962). At that time, sys- in interest coincides with declining funds for pro- tematic procedures for measuring glacier mass bal- grams to monitor glacier mass balance. In light of ance were being developed and culminated in the the renewed interest in mass balance data and fis- International Hydrological Decade (IHD; 1965– cal pressures, the International Commission on 1974) project, which examined combined heat, ice, Snow and Ice is convening a workshop to address and water balances at selected glacier basins around techniques of measuring glacier mass balance and the world (UNESCO 1970). This program became methods to model mass balance.

29 Tarfala Research Station Annual Report 1997–98

The specific goals of the workshop include, measurements that represent different altitude 1. Approaches to measuring and modelling “prob- bands. To assess the effect of climate variations on lem“ glaciers, including large glaciers (greater than whole glaciers, volume estimates alone may be suf- 50 km2), debris covered glaciers, calving glaciers, ficient. The approach to the measurements depends highly crevassed glaciers, and glaciers where abla- on the climatic environment in which the glacier tion/accumulation periods do not normally coin- exists. Traditionally in the northern temperate cli- cide with the summer and winter seasons; mates, we regard glaciers as having a single accu- 2. Alternative methods for measuring mass bal- mulation season (winter) and a single ablation sea- ance including remote sensing, flux divergence, vol- son (summer) and our approach and many of those ume change; found in the literature is derived from that perspec- 3. Strategies for reduced field programs; and tive. One has to remember that glaciers in differ- 4. Analysis of errors in all methods. ent climates have different mass balance regimes, from polar glaciers where ablation occurs all year Organisation long with sporadic accumulations at any time and The organising committee included Andrew Foun- is storm dependent, to tropical glaciers that ablate tain (chair), Mark Dyurgerov, Peter Jansson (local all year long and have two periods of accumula- organiser, editor for the proceedings volume), and tion (Kaser, GA). Specific methods will also differ Georg Kaser. for different climatic regimes where in one case The Workshop seasonal accumulation of snow is 10 m thick or 0.1 m thick. The workshop was convened from 10 to 12 Au- In spite of these different motivations and vari- gust in Tarfala. The workshop included 20 oral able climatic conditions a number of broad rec- papers each allotted 30 minutes for presentation ommendations and discussions developed. To be including questions over about 1.6 days. Because clear, these conclusions are based on the examina- of the generous schedule and lack of simultaneous tion of past data sets, long time series of data, and sessions each paper could be discussed fully by all the application of new methods and technologies participants. Also, because of the relative isolation with out any of which this would not have been of the field station and that all meals were taken possible. together in the same dining room, discussions could be continued throughout the day and evening. In Recommendations addition to the presentations, two short field trips 1. Direct methods to assess glacier mass balance, to the moraines around Isfallglaciären and on to which include stake, snow pit, and probing meas- Storglaciären were part of the program. Each trip urements, need to be checked using volume esti- required only a few minute walk from the station mates from geodetic changes in the surface eleva- and were quite useful to illustrate various points tion of the glacier. Although all the causes are un- raised from the presentations. clear at this time, direct methods are susceptible to Of the 20 oral presentations, 19 papers were systematic errors. See articles in GA by Andreassen, submitted for publication and will be included in Krimmel, and Østrem and Haakensen. However, the forthcoming proceedings volume, published as not all glaciers have such differences between di- a regular issue of Geografiska Annaler (abbrevi- rect and volume methods. ated GA in the following) during 1999 (see pre- 2. When reporting the results of mass balance liminary list of papers below). In addition to these measurements, either as data reports or peer re- reports other submissions are included from au- viewed journal articles, it is vital to include, thors who were not able to attend the workshop. a. Error estimates. Given that glacier mass balance On the last day of the meeting the participants tends toward zero in an equilibrium conditions an spent the morning discussing the results of the pre- estimate of the error is important for the reliability vious presentations. It was difficult to make spe- of the calculation and the sign of the final value. cific recommendations because the reason for mak- Also it is vital for estimates of water runoff and, ing mass balance measurements largely control the ultimately, sea level rise. kind of measurements made. For example, some b. Be clear on the methodology used to measure mass balance programs are funded by water power and calculate mass balance. As Dyurgerov and agencies to estimate how much water is coming Meier (GA) point out different methods can pro- from different parts of a glacier (Østrem and duce quantities that sound similar but in fact are Haakensen, GA). Therefore, one needs to make not comparable (e.g. winter mass balance versus

30 Tarfala Research Station Annual Report 1997–98 net annual accumulation) and therefore can not be Discussions mixed when determining mass change with time. A number of topics were discussed and no clear c. When reporting results we recommend that recommendations were made. However, the points standard plots are used where altitude is given on of the discussion were deemed valuable to include the vertical axis and balance on the horizontal axis. here. One such topic was the hydrological method Included with the net balance curve are the sum- to assess glacier mass balance. The total mass bal- mer and winter balance curves and data points used ance of a glacier can be found by calculating the to construct the measured curves (see Østrem and difference between runoff from the glacier and pre- Brugman, 1992). cipitation over the glacier basin. In principle this d. Tables of mass balance with elevation need to technique is quite simple and straightforward, in be included for summer, winter, and yearly (net or practice, however, it can be quite challenging. As- annual) balance (see Østrem and Brugman, 1992). suming one can accurately measure annual stream- 3. Repeated vertical aerial photography should flow, itself challenging and labour intensive par- be included in a mass balance program whenever ticularly in a glacial environment, significant possible. The photographs provide a data source problems are encountered in accurately determin- for photogrammetric mapping of the glacier to- ing the spatial distribution of precipitation. Another pography that can be accessed at any time. Satel- problem is encountered by the temporary storage lite images in the visible spectrum can also be used of water in a glacier (Tangborn et al. 1971). O. in the same way if the resolution is sufficient. Also Reinwarth showed a graph of annual balance well the photographs can be used almost directly to in- correlated with summer runoff. Some participants fer changes in glacier area and provide a sense of were of the opinion that the hydrological method conditions. Of course, the photographs should be should never be used while others argued that in acquired near the end of the summer to minimize the absence of any other information it could be seasonal snow cover. useful. It seems unlikely to us that precipitation 4. Volume methods, which utilize techniques as measurements of sufficient reliability and spatial laser altimetry (Favey and others, GA; Echelmeyer distribution will be available without measurements at al., IGS), photogrammetry (Andreasssen GA; of the glacier. In any event, rapidly new methods Krimmel GA), and global positioning systems (e.g. and technologies as discussed in these articles will Hagen et al. GA), provide important measures of probably render these arguments moot. glacier change. Such methods can be used to rap- The participants generally agreed that intensive idly assess changes in glaciers over long time peri- sampling of mass balance variations on glaciers is ods. They do not, however, replace direct methods probably not necessary for total mass balance or where mass balance versus altitude information is mass balance gradients. While networks of 5–10 required (e.g. water flow; climate modeling). As stakes are sufficient for smaller valley glaciers net- shown by Gudmunsson and Bauder (GA), the vol- works of 10–20 stakes are sufficient for larger gla- ume change and specific mass balance for a glacier ciers (e.g. Fountain and Vecchia GA; Hoch and is a combination of both glacier dynamics and sur- Jensen GA; Jansson GA; Hagen et al. GA). As long face mass exchange (local mass balance) because as mass balance variations are dominated by el- one has to consider the changing area of the gla- evation, which is typically the case for valley gla- cier. The mass balance at a point, or its gradient ciers, a line of stakes up the glacier extending over with altitude is the climate signal, without dynamic the elevation range of the glacier is sufficient. More influence. generally, total mass balance of a glacier is insensi- 5. New methods of remotely assessing glacier tive to small variations in input variables. Given mass balance using flux divergence calculations that scaling relations exist between glacier length, based on surface velocity derived from photogram- area, volume (Bahr, 1997) one might expect the metry (Rasmussen and Krimmel GA; Gudmundsson existence of some scale for stake networks. and Bauder GA) provide new opportunities to evaluate glaciers too difficult to measure directly Final Word either because of their large size and/or difficult Many of the analyses presented in this workshop terrain. It is critical to test these methods and new would not have been possible without the mainte- methods in general against traditional methods on nance of long time series of glacier measurements glaciers where long mass balance time series has at individual glaciers. The value of these data sets been established.

31 Tarfala Research Station Annual Report 1997–98 increase proportionately to their length and their ciers (>100 km2) require application of new meth- maintenance is important not only to evaluate and odologies presented in this volume because direct possibly correct past estimations with new infor- methods are too slow and costly for large areas. mation, but to understand the response of glaciers Also new methods, along the lines of Nakawo (GA) to climatic (annual, decadal, and hopefully cen- will be required to assess the mass balance of de- tury) variations and its subsequent effect on haz- bris covered glaciers of the Himalayas. For these ards, runoff, and sea level change. We need to con- reasons a program of simple measurement pro- tinue these monitoring programs, they are vital to grams needs to be developed to assess the global our understanding. effect of glaciers on sea level change. In our effort to understand glacial processes our Acknowledgements observations are woefully under represented. Ap- proximately 50% of the glacier observations are The workshop was primarily sponsored by the In- in Europe, which contains only about 2% of the ternational Commission for Snow and Ice (ICSI), glacier cover of the world (Meier pers comm). For Tarfala Research Station and the Department of the purpose of hydroelectric power development Physical Geography, Stockholm University. Finan- this emphasis is reasonable. On the contrary, for cial support for publication of the workshop pro- the purpose of global sea level change important ceedings was graceously provided by the National regions of the world are virtually ignored. To bet- Science Foundation, The Wenner-Gren Founda- ter assess the contribution of glaciers to sea level tions (Sweden), and the Carl Mannerfelt Fund we require a more random sampling of all size (Sweden). Thanks are due to Emeritus Professor J. ranges of glaciers rather than the convenient gla- O. Mattsson, Chief Editor of Geografiska Annaler ciers we monitor today. Simple measurements on (thereby also acknowledging the indirect support these glaciers supported by scaling theory is the from the Swedish Society for Anthropology and most cost effective approach. For the larger gla- Geography, SSAG) for the support provided throughout the publishing process.

Figure 1. Workshop participants (from the top left): Oskar Reinwarth, Per Holmlund, David Collins, Gerog Kaser, Al Rasmussen, Dave Morse, Liss Andreassen, Jon Ove Hagen, Masayoshi Nakawo, Gunnar Østrem, Roger Braithwaite, Bob Krimmel, Andrew Fountain, Regine Hock, Etienne Favey, Andreas Bauder, Mark Dyurgerov, and Peter Jansson

32 Tarfala Research Station Annual Report 1997–98

References W. Haeberli, R. Frauenfelder, M. Hoelzle & M. Maisch: Rates and acceleration trends of global glacier mass Bahr, D., 1997: Global distribution of glacier proper- changes ties: a stochastic scaling paradigm. Water Resources J. O. Hagen, K. Melvold, T. Eiken, E. Isaksson, & B. Research, 33: 1669–1679. Lefauconnier Mass balance methods on Kongsvegen, IGS (International Glaciological Society), 1962: Sym- Svalbard. posium on Problems of Mass Balance Studies, J. E. Heucke: A light portable steam-driven ice drill suit- Glaciol. 4: 251–318. able for drilling holes in ice and firn. IGS (International Glaciological Society), 1990: Proceed- R. Hock, & H. Jensen: Application of kriging interpo- ings of the Symposium on Ice and Climate, Ann. lation for glacier mass balance computations. Glaciol., 14. P. Holmlund & P. Jansson: The Tarfala mass balance IGS (International Glaciological Society), 1998: Proceed- program ings of the Symposium on Antarctica and Global P. Jansson: Effect of uncertainties in measured variables Change, Hobart, Ann. Glaciol., 27. on the calculated mass balance of Storglaciären. Oerlemans, J. (Ed). 1989: Glacier fluctuations and cli- G. Kaser & C. Georges: On the mass balance of low mate change. Kluwer Academic Publishers, Amster- latitude glaciers with particular consideration of the dam. Peruvian Cordillera Blanca Østrem G., and Brugman M., 1991: Glacier mass-bal- R. M. Krimmel: Analysis of difference between direct ance measurements. National Hydrology Research and geodetic mass balance measurements at South Institute Report 4. Environment Canada, Saskatoon. Cascade Glacier, Washington.. UNESCO, 1970: Combined heat, ice and water bal- M. Kuhn, E. Dreiseitl, S. Hofinger, G. Markl, N. Span, ances at selected glacier basins. United Nations Edu- & G. Kaser,: Measurements and models of the mass cational, Scientific and Cultural Organizaion, Paris. balance of Hintereisferner ZGG (Zeitschrift für Gletscherkunde und Glazial- M. M. Miller & M. S. Pelto: Mass balance measure- geologie), 1997: Proceedings of the Symposium on ments on the Lemon Creek Glacier, Juneau Icefield Glacier Mass Balances, Zeitschrift für Gletscher- Alaska 1953–1995. kunde und Glazialgeologie. volumes 33 and 34. D. L. Morse, E. D. Waddington, H.P. Marshall, T.A. Tangborn 1971 Neumann, J. Dibb, D. Winebrenner, & E. J. Steig, Workshop papers (See Geogr. Ann. for com- Accumulation rate measurements at Taylor Dome, East Antarctica: Techniques and strategies for mass plete and final references) balance measurements in polar environments. L. M. Andreassen: Comparing traditional mass balance M. Nakawo & B. Rana: Estimate of ablation rate of measurements with long-term volume change ex- glacier ice under a supraglacial debris layer. tracted from topographical maps: a case study of G. Østrem & N. Haakensen: Map comparisons or tra- Storbreen glacier in Jotunheimen, Norway, in the ditional mass balance measurements: Which method period 1940–1997. is better? A. Arendt: Approaches to Modelling the Mass Balance V. V. Popovnin, Annual mass-balance series of a tem- of High Arctic Glaciers. perate glacier in the Caucasus, reconstructed from R. J. Braithwaite: Modelling mass balance changes that an ice core. may occur as a result of climate changes. L. A. Rasmussen & R. M. Krimmel: Using vertical aerial J. G. Cogley: Effective sample size for glacier mass-bal- photography to estimate mass balance at a point. ance. N. Reeh: Mass balance of the Greenland ice sheet: can H. Conway, L. A. Rasmussen & H.-P. Marshall Annual new remote sensing techniques reduce the uncer- Mass Balance Of Blue Glacier, U.S.A.: 1955–97. tainty? M. N. Demuth & A. Pietroniro, Glacier monitoring and O. Reinwarth & H. Escher-Vetter, Mass balance of climate change detection using RADARSAT - Re- Vernagtferner, Austria from 1964/65 to 1996/97: Re- sults from Peyto Glacier, Canada. sults for three sections the entire glacier. M. Dyurgerov & M. Meier: Analysis of winter and sum- D. C. Trabant: Mass-balance measurements in Alaska mer glacier mass balances. and suggestions for simplified observation programs E. Favey, A. Geiger, G H. Gudmundsson, & A. Wehr: W. H. Theakstone, F. M. Jacobsen, & N. T. Knudsen, Evaluating the potential of an airborne laser scan- Changes of snow cover thickness measured by con- ning system for measuring volume changes of gla- ventional mass balance methods and by global posi- ciers. tioning system surveying. A. G. Fountain & A. V. Vecchia: How many ablation W. Tangborn, A method to calculate glacier mass bal- stakes are required to measure the mass balance of a ance from its area-altitude distribution and low-al- glacier? titude meteorological observations G. H. Gudmundsson & A. Bauder: Towards an indirect X. Zichu, H. Jiankang, L. Chaohai, & L. Shiyin: Meas- determination of the mass balance distribution of urement and estimative models of glacier mass bal- glaciers using the kinematic boundary condition. ance in China.

33 Tarfala Research Station Annual Report 1997–98 Literature concerning the Tarfala valley and its close surroundings

Revised version, May 17 1999

New papers 1997 and 1998 Holmlund, P., 1998. Glacier mass balance and ice-core records from northern Sweden. Ambio. 27(1): 266- Braithwaite, R. J. and Zhang, Y., 1999. Modelling 269. changes in glacier mass balance that may occur as a Holmlund, P. and Jansson P., 1999. The Tarfala mass result of climate changes. Geografiska Annaler. 81A balance program. Geografiska Annaler. 81A (4): xx- (4): xx-xx. xx. Cutler, P., 1998. Modelling the evolution of subglacial Holmlund, P., and Schneider, T., 1997. The effect of tunnels due to varying water input. Journal of continentality on glacier response and mass balance. Glaciology. 44 (148): 485-497. Annals of Glaciology. 24: 272-276. Dowdeswell, J. A., Hagen, J. O., Björnsson, H., Hooke, R. LeB., Hansson, B., Iverson, N. R., Jansson, Glazovsky, A. F., Harrison, W. D., Holmlund, P., P. and Fischer, U. H., 1997. Rheology of till beneath Jania, J., Koerner, R. M., Lefauconnier, B., Storglaciären, Sweden. Journal of Glaciology. 43 Ommanney, C. S. L. and Thomas, R. H., 1997. The (143): 172-179. mass balance of circum-artic glaciers and recent cli- Iversen, N. R., Hooyer, T. S. and Baker, R. W., 1998. mate change. Quarternary Research. 48: 1-14. Ring-shear studies of till deformation: Coulumb- Fountain, A. G. and Walder. J. S., 1998. Water flow plastic behavior and distributed strain in glacier beds. through temperate glaciers. Reviews of Geophysics. Journal of Glaciology. 44 (148): 31-40. 36, 3: 299-328. Iversen, N. R., Baker, R. W., H Hooke, R. LeB., Hansson, Fischer, U. H., Iversson, N. R., Hanson, B., Hooke, R. B., and Jansson, P., 1999. Coupling between a gla- LeB. and Jansson, P., 1998. Estimation of hyraulic cier and a soft bed: 1. A relation between effective properties of subglacial till from ploughmeter meas- pressure and local shear stress determined from till urements. Journal of Glaciology. 44 (148): 517-522. elasticity. Journal of Glaciology. 45 (149): 634-642. Haeberli, W., 1997. Fluctuation of Glaciers 1990-1995. Jansson, P., 1997. Longitudinal coupling effects in ice A compilation of national reports to “the Perma- flow across a subglacial ridge. Annals of Glaciology. nent Service on the Fluctuations of Glaciers of the 24: 169-174. IUGG – FAGS/ICSU“, 296p. Jansson, P., 1999. Effects of uncertainties in measured Haeberli, W., Hoelzle, M. and Bösch, H., 1997: Glacier variables on the calculated mass balance of mass balance bulletin. A contribution to the Global Storglaciären. Geografiska Annaler. 81A (4): xx-xx. Environment Monitoring System (GEMS) and the Jansson, P., Richardsson, C. and Jonsson, S., 1999. as- International Hydrological Programme. IAHS(ICSI)- sessment of requirments for cirque formation in UNEP-UNESCO. Bulletin No. 4 (1994-1995). northern Sweden. Annals of Glaciology. 28: xx-xx. Hanson, B., Hooke, R. LeB. and Grace, Jr, E. M., 1998. Karlén, W., 1998. Climate variations and the enhanced Short-term velocity and water-pressure variations greenhouse effect. AMBIO. 27(4): 270-274. down-glacier from a riegel, Storglaciären, Sweden. Oerlemans, J., Anderson, B., Hubbard, A., Huybrechts, Journal of Glaciology. 44 (147): 359-367. Ph., Johannesson, T., Knap, W. H., Schmeits, M., Hock, R. 1998. Modelling of glacier melt and discharge Stroeven, A. P., van de Wal, R. S. W., Wallinga, J. 1998, Züricher Geographische Schriften, Depart- and Zou, Z., 1998. Modelling the respons of gla- ment of Geography, ETH Zürich. 140 pp. ciers to climate warming. Climate Dynamics. 14: Hock, R. 1999: A distributed temperature-index ice- and 267-274. snowmelt model including potential direct solar ra- Pohjola, V. A. and Rogers, J. C., 1997. Atmospheric diation. Journal of Glaciology. 45(148). 101-111. circulation and variations in Scandinavian mass bal- Hock. R. and Noetzli, C., 1997, Areal melt and dis- ance. Quaternary Research. 47(1): 29-36. charge modelling of Storglaciären, Sweden. Annals Pohjola, V. A. and Rogers, J. C., 1997. Coupling be- of Glaciology. 24: 211-216. tween the atmospheric circulation and extremes of Holmlund, P., 1997. Climatic influence on the size of the mass balance of Storglaciären, northern Scandi- glaciers in Northern Sweden during the last two cen- navia. Annals of Glaciology. 24: 229-233. turies. In Frenzel, B., et al. (eds.) Glacier fluctua- tions during the holocene. ESF project, European paleoclimate and man 16. Paläoklimat-forschung band 24, Zürich: 115-124.

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Papers published after 1980 Fountain, A. G. and Walder. J. S., 1998. Water flow through temperate glaciers. Reviews of Geophysics. Ackert, R., 1984. Ice-cored lateral moraines in Tarfala 36, 3: 299-328. Valley, Swedish Lappland. Geografiska Annaler. 66A Fuenzalida, H. and Holmlund, P., 1995. Anomalous (1–2): 79–88. responses to 20th century climatic changes in the Andreasson, P.-G., and Gee, D. G., 1989. Bedrock geol- Darwin Cordilliera, southern Chile. Journal of ogy and morphology of the Tarfala area, Kebnekaise Glaciology, 41 (139): 465-473. Mts., Swedish Caledonides. Geografiska Annaler. Grove, J.M., 1988. The Little Ice Age. 498 p, Methuen 71A (3–4): 235–239. & Co, London. Björnsson, H., 1981. Radio-echo sounding maps of Grudd, H., 1990. Small glaciers as sensitive indicators Storglaciären, Isfallsglaciären and Rabots Glaciär, of climatic fluctuations. Geografiska Annaler. 72A northern Sweden. Geografiska Annaler. 63A (3–4): (1): 119–123. 225–231. Grudd, H. and Schneider, T., 1996. Air temperature at Bodin, A., 1993. Physical properties of the Kårsa gla- Tarfala Research Station 1946-1995. Geografiska cier, Swedish Lapland. Naturgeografiska institu- Annaler, 78A (2-3): 115-120. tionen vid Stockholms universitet, Forskningsrapport Günter, R., and Widlewski, D., 1986. Die korrelation nr 97, (ISSN 0346-7406), 18p. verschiedener Klimaelemente mit dem Brand, G., Pohjola, V., and Hooke, R. LeB., 1987. Evi- Massenhaushalt alpiner und Skandinavischer dence for a till layer beneath Storglaciären, Sweden, Gletscher. Zeitschrift für Gletscherkunde und based on electrical resistivity measurements: Jour- Glazialgeologie 22 (2): 125–147. nal of Glaciology. 33 (115): 311–314. Haeberli, W., 1985. Fluctuation of Glaciers 1975–1980. Braithwaite, R. J. and Zhang, Y., 1999. Modelling A compilation of national reports to “The Perma- changes in glacier mass balance that may occur as a nent Service on the Fluctuations of Glaciers of the result of climate changes. Geografiska Annaler. 81A IUGG – FAGS/ICSU“, 265 p. (4): xx-xx. —1987. Fluctuation of Glaciers 1980–1985. A compi- Bronge, C., 1985. Hydrologisk verksamhet i Tarfala, lation of national reports to “the Permanent Service 1974–1982. Dept. Physical Geography, University on the Fluctuations of Glaciers of the IUGG – FAGS/ of Stockholm Forskningsrapport 62, (ISSN 0346- ICSU“. 7406), 81 p. —1993. Fluctuation of Glaciers 1985-1990. A compi- —1996. The excavation of the Storglaciären trough lation of national reports to “the Permanent Service during Quaternary. Geografiska Annaler 78A (2-3): on the Fluctuations of Glaciers of the IUGG – FAGS/ 163-170. ICSU“, 322 p. Brzozowski, J., and Hooke, R. LeB., 1981. Seasonal —1997. Fluctuation of Glaciers 1990-1995. 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Hanson, B., Hooke, R. LeB. and Grace, Jr, E. M., 1998. the holocene. ESF project, European paleoclimate Short-term velocity and water-pressure variations and man 16. Paläoklimatforschung band 24, Zürich. down-glacier from a riegel, Storglaciären, Sweden. 115-124. Journal of Glaciology. 44 (147): 359-367. —1998. Glacier mass balance and ice-core records from Herzfeld, U. C., Eriksson, M. G. and Holmlund, P., 1993. northern Sweden. Ambio. 27(1): 266-269. On the Influence of Kriging Parameters on the Car- Holmlund, P., and Eriksson, M., 1989. The cold sur- tographic Output—A study in Mapping Subglacial face layer on Storglaciären. Geografiska Annaler. Topography. Mathematical Geology 25 (7): 881– 71A (3–4): 241–244. 900. Holmlund, P., and Hooke, R. LeB., 1983. High water- Hock, R. 1998. 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Hooke, R. LeB., and Iverson, N., 1985. Experimental —1996: Dynamics and hydrology of a small polythermal study of ice flow around a bump, comparison with valley glacier. Geografiska Annaler, 78A (2-3): 171- theory. Geografiska Annaler. 67A (3–4): 187–197. 180. Hooke, R. LeB., Holmlund, P., and Iverson, N. R., 1987. —1997. Longitudinal coupling effects in ice flow across Extrusion flow demonstrated by borehole deforma- a subglacial ridge. Annals of Glaciology. 24: 169- tion measurements over a riegel, Storglaciären, Swe- 174. den. Journal of Glaciology. 33 (113): 72–78. —1999. Effects of uncertainties in measured variables Hooke, R. LeB., Miller, S. B., and Kohler, J., 1988. Char- on the calculated mass balance of Storglaciären. acter of the englacial and subglacial drainage sys- Geografiska Annaler. 81A (4): xx-xx. tem in the upper part of the ablation area of Jansson, P., and Hooke, R. LeB., 1989. Short-term vari- Storglaciären, Sweden. 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—1996. Simulation of particle paths and deformation —1985. Glaciologi. Kosmos 62: 109–124. of ice structures along a flow-line on Storglaciären, —1993. Glaciers of Europe - Glaciers of Sweden. In, Sweden. Geografiska Annaler, 78A (2-3): 181-192. Satellite image atlas of glaciers of the world (eds. Pohjola, V. A. and Rogers, J. C., 1997. Atmospheric Williams, R.S. and Ferrigno, J.G.), U.S. Geological circulation and variations in Scandinavian mass bal- survey professional paper 1386-E, Washington, ance. Quaternary Research. 47(1): 29-36. 1993. E-4: 111–125. Pohjola, V. A. and Rogers, J. C., 1997. Coupling be- Seaberg, S. Z., Seaberg, J. Z., Hooke, R. LeB., and tween the atmospheric circulation and extremes of Wiberg, D., 1988. Character of the englacial and the mass balance of Storglaciären, northern Scandi- subglacial drainage system in the lower part of the navia. Annals of Glaciology. 24: 229-233. ablation area of Storglaciären, Sweden, as revealed Radok, U., 1980. Climatic background to some glacier by dye trace studies: Journal of Glaciology. 34 (117): fluctuations. World Glacier Inventory. Proceedings 217–227. of the Riederalp Workshop, September 1978. IAHS- Seppälä, M.,(et al), 1989. Glaciological course in Tarfala. AISH Publ. 126: 295–304. Terra 101 (3): 252–274. Rafstedt, T., 1983. Vegetationskarta över de svenska Skrivastava, H. B., Huddlestone, P. and Earley, D., 1995. fjällen. Kartblad nr 5 Kebnekaise (29 I). Naturgeog. Strain and possible volume loss in a high-grade duc- inst. Stockholms univ. tile shear zone. Journal of Structural Geology. 17 Raper, S.C.B., Briffa, K.R. and Wigley, T.M.L., 1996. (9): 1217-1231. Glacier change in northern Sweden from AD 500: a Stroeven, A.P., 1996. The robustness of one-dimensional, simple geometric model of Storglaciären. Journal of time dependent, ice-flow models: A case study from Glaciology. 42 (141): 341-351. Storglaciären, northern Sweden. Geografiska Reynaud, L., Vallon, M., Martin, S., and Letreguilly, Annaler 78A (2-3): 133-146. A., 1984. Spatio temporal distribution of the glacial Stroeven, A.P., and van der Wal, R.S., 1987. Mass bal- mass balance in the Alpine, Scandinavian and Tien ance and flow of Rabots glaciär; A comparison with Shan areas. Geografiska Annaler. 66A (3): 239–247. Storglaciären. Dept. Physical Geography, University Richardson, C. and Holmlund, P., 1996. Glacial cirque of Stockholm. Forskningsrapport 64, (ISSN 0346- formation in northern Sweden. Annals of Glaciology 7406), 99 p. 22: 102-106. —1990. A comparison of the mass balances and flows Rosqvist, G., and Östrem, G., 1989. The sensitivity of a of Rabots glaciär and Storglaciären, Kebnekaise, small ice cap to climatic fluctuations. Geografiska northern Sweden. Geografiska Annaler. 72A (1): Annaler. 71A (1–2): 99–104. 113–118. Schneider, T., 1994. Water movement and storage in the Walford, M. E. R., and Kennett, M. I., 1989. A firn of Storglaciären, northern Sweden. Forknings- synthetic-aperture radio-echo experiment at rapport STOU-NG 99, (ISSN 0346-7406), 89 p Storglaciären, Sweden. Journal of Glaciology. 35 Schneider, T., and Bronge, C., 1992. Suspended sedi- (119): 43–47. ment transport and discharge of Tarfalajåkk, the Walford, M., Kennett, M. I., and Holmlund, P., 1986. proglacial stream of Storglaciären, Northern Swe- Interpretation of radio echoes from Storglaciären, den, 1980–1990. Forskningsrapport STOU-NG 92, northern Sweden. Journal of Glaciology. 32 (110): (ISSN 0346-7406), 28 p. 39–49. —1996. Suspended sediment transport in the Åmark,M., 1980. Glacial flutes at Isfallsglaciären, Storglaciären drainage basin. Geografiska Annaler, Tarfala, Swedish Lapland. Geologiska Föreningens 78A (2-3): 155-162. Förhandlingar (GFF). 102 (3): 251–259. Schytt, V., 1981. The net mass balance of Storglaciären Östling, M., and Hooke, R. LeB., 1986. Water storage related to the height of the equilibrium line and to in Storglaciären, Kebnekaise, Sweden. Geografiska the height of the 500 mb surface. Geografiska Annaler. 68A (4): 279–290. Annaler. 63A (3–4): 219–223

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Eckerbom, E. and Palosuo, E., 1963. A study of ice crys- —1975. Lichenometrisk datering i norra Skandinavien tals at Storglaciären, Kebnekajse. in: Kingery, W. D. – metodens tillförlitlighet och regionala tillämpning. (ed.): Ice and snow, properties, processes, and ap- Naturgeografiska institutionen, Stockholms univ. plications. Proc. Conf. Mass. Inst. Tech., M.I.T. Press. Forskningsrapport 22, (ISSN 0346-7406), 67 p. 56-62. —1976. Holocene climatic fluctuations indicated by gla- Ekman, S.-R., 1961. Thermal Drilling in Isfallsglaciären, cier and tree-limit variations in northern Sweden. Kebnekajse. Geografiska Annaler. 43 (3–4): 422– Naturgeografiska institutionen, Stockholms univ. 423. Forskningsrapport 23, 7p. Grainger, M. E. and Lister, H., 1966: Wind speed, sta- Karlen, W., and Denton, G. H., 1975. Holocene glacial bility and eddy viscosity over melting ice surfaces. variations in Sarek National Park, northern Sweden. Journal of Glaciology. 6 (43): 101–127. Boreas 5: 25–56. Hamberg, A., Rabot, C., and Mercanton, P. L., 1930. Kasser, P., 1967. Fluctuations of glaciers 1959–1965. A Commission UGGI des glaciers: Rapport pour contribution to the International Hydrological Dec- 1914–1928. Venezia 1930. 1–53. ade. IASH (ICSI) UNESCO, 52 p. Herrmann E., 1931. Gletscherstudien im Kebnekaise- — 1973. Fluctuation of Glaciers 1965–1970. A compi- Gebiet (Schwed. Lappland). Zeitschrift für lation of national reports to “The Permanent Serv- Gletscherkunde. 19: 263–284. ice on the Fluctuations of Glaciers of the IUGG – Hoinkes, H., 1967. Gletscherschwankungen und Wet- FAGS/ICSU“, 357 p. ter in den Alpen. In: Karin Schrom and J. C. Thams King, L., 1976. Permafrostuntersuchungen in Tarfala (eds.): Veröffentlichen der Schweizerischen (Schwedisch Lappland) mit Hilfe der Hammerschlag- Meteorologischen Zentralanstalt nr. 4. ( seismik. Zeitschrift für Gletscherkunde und Glazial Internatianale tagung für alpine ,eteorologie. In Brig geologie 12 (2): 187–204. und Zermatt 14–17 sept 1966. City-druck AG, Kulling, O., 1964. Översikt över norra Zürich. 9–24. Norrbottensfjällens kaledonberggrund. Sveriges —1968. Glacier variation and weather. Journal of geologiska undersökning (SGU), Ba 19: 166 p. Glaciology. 7 (49): 3–19. Mannerfelt, C. M:son., 1939. Geografiska bilder. Ymer Hoppe, G., 1960. Glacial morphology and inland ice 59: 162–166. recession in Northern Sweden. Geografiska Annaler. —1940. Storglaciärens tillbakagång i Kebnekaise. Ymer 41: 193–212. 60 (1): 60–61. —1961. Naturgeografisk fältstation i Kebnekaise. Melander, O., 1975. Geomorfologiska kartbladet, 29 I Svensk Geografisk Årsbok 37: 224–225. Kebnekaise. Beskrivning och naturvärdes- —1963. I den stora landisens spår: terrängformer i bedömning. SNV PM 540. 78 p. Lappland. Natur i Lappland 1: 130–144. Müller, F., 1977. Fluctuation of Glaciers 1970–1975. A —1969. Norrlandsälvarnas naturvärden. Värdegraderad compilation of national reports to “The Permanent bedömning av Torne, kalix, Pite älvars samt Service on the Fluctuations of Glaciers of the IUGG Vindelälvens betydelse för forskning och turism. – FAGS/ICSU“, 269 p. Statens naturvårdsverk. Del II av PU 20.11.1969: Nilsson, J., and Sunblad, B., 1975. The internal drain- 3–27. age of Storglaciären and Isfallsglaciären described Hoppe, G., and Ekman, S.-R., 1964. A note on the allu- by an autoregressive model. Geografiska Annaler. vial fans of Ladtjovagge, Swedish Lapland. 57A (1–2): 73-98. Geografiska Annaler. 46 (3): 338–342. Nye, J. F., 1965. The frequency response of glaciers. Hoppe, G., and Schytt, V., 1953. Some observations on Journal of Glaciology. 5 (41): 567–587. fluted moraine surfaces. Geografiska Annaler. 35 (2): Nye, J. F., 1965. A numerical method of inferring the 105–115. budget history of a glacier from its advance and re- Hoppe, G., Schytt, V., and Strömberg, B., 1965. Från treat. Journal of Glaciology. 5 (41): 589–607 fält och Forskning Naturgeografi vid Stockholms Quensel, P., 1919. De kristallina sevebergarternas Universitet. Ymer (3–4): 109–125 geologiska och petrografiska ställning inom Håkansson, T., 1955. Anteckningar om flora och veg- Kebnekajseområdet. Geologiska Föreningens i etation i Kebnekajseområdet. Botaniska notiser 108 Stockholm Förhandlingar (GFF) 41: (2): Rapp, A., 1959. Avalanche Boulder Tongues in Johansson, H. F., 1951. Scientific investigations in the Lappland. Geografiska Annaler. 41 (1): 34–48. Kebnekajse Massif, Swedish Lappland. II. The pe- Schytt, V., 1947. Glaciologiska arbeten i Kebnekajse. trology and tectonics of the Kebnekajse region and Ymer 67 (1): 18–42. their morphological importance. Geografiska —1949. Re-freezing of meltwater on the surface of gla- Annaler. 33 (1–2): 95–120. cier ice. Geografiska Annaler. 31 (1–4): 222–227. Jonsson, S., 1970. Structural studies of subpolar glacier —1959. The Glaciers of the Kebnekajse-Massif. Geo- ice. Geografiska Annaler. 52A (2): 129–145. grafiska Annaler. 41 (4): 213–227. —1973. Registration of a sudden vertical displacement —1960. Regime studies on Storglaciären, Kebnekajse of the ice surface of Isfallsglaciären, Northern Swe- during 1960. Geografiska Annaler. 42 (1): 62–63. den. Geografiska Annaler. 55A (1): 64–68. —1961. Notes on Glaciological activities in Kebnekajse, Karlen, W., 1973. Holocene glacier and climatic varia- Sweden. Regime studies on Storglaciären, tions, Kebnekaise mountains, Swedish Lapland. Kebnekajse, during 1961. Geografiska Annaler. 43 Geografiska Annaler. 55A (1): 29–63. (3–4): 420–421

39 Tarfala Research Station Annual Report 1997–98

—1962. Naturgeografisk fältstation i Kebnekajse. Stenborg, T., 1965. Problems concerning winter run-off Svensk Naturvetenskap, 332–345. from glaciers. Geografiska Annaler. 47A (3): 141– —1962. Mass balance studies in Kebnekajse. Journal 184. of Glaciology. 4 (33): 281–286. —1969. Studies of the internal drainage of glaciers. —1962. Mass balance studies on Storglaciären during Geografiska Annaler. 51A (1–2): 13–41. 1962. Geografiska Annaler. 44 (3–4): 407–409. —1973. Some viewpoints on the internal drainage of —1962. A tunnel along the bottom of Isfallsglaciären. glaciers. SymposiumontheHydrology of Glaciers. Geografiska Annaler. 44 (3–4): 411–412. Cambridge, 7–13 September 1969, organized by the —1963. Fluted moraine surfaces. Journal of Glaciology. Glaciological society. Publication no. 95. 1973, 117– 4 (36): 825–827. 130. —1965. Notes on glaciological activities in Kebnekaise, Stork, A., 1963. Plant Immigration in front of Retreat- Sweden during 1964. Geografiska Annaler. 47A (1): ing Glaciers,with examples from the Kebnekajse 65–71. Area,Northern Sweden. Geografiska Annaler. 45 (1): —1966. Notes on glaciological activities in Kebnekaise, 1–22. Sweden – 1965. Geografiska Annaler. 48A (1): 43– —1963. Några bidrag till kännedomen om 50. Kebnekajseområdets kryptogamflora. Botaniska —1967. A study of “Ablation Gradient“. Geografiska notiser 116 (1): 11–15. Annaler. 49A (2–4): 327–332. Svenonius F., 1910. Die gletscher Schwedens im Jahre —1968. Notes on glaciological activities in Kebnekaise, 1908. Sveriges Geologiska Undersökningar (SGU) Sweden during 1966 and 1967. Geografiska Annaler. serie Ca 5 part I: 1–54. 50A (2): 111–120. Vilborg, L., 1977. The cirque forms of Swedish Lapland. —1968. Tarfalajåkkas vattenföring och slamtransport Geografiska Annaler, 59A (3-4): 89-150. 1966–1967. Naturgeografiska inst. Stockholms Woxnerud, E., 1951. Scientific investigations in the universitet. Forskningsrapportserien STOU-NG 3 Kebnekajse Massif, Swedish Lappland. III. (ISSN 0346-7406), 24 p. Kartografiska arbeten i Kebnekajse. IV. Det lokala —1970. De svenska glaciärernas vittnesbörd. In: triangelnätets i Kebnekajse anslutning till riksnätet. Ahlmann m fl Klimatologiska förändringar omkring Syd- och nordtopparnas höjd över havet. Nordatlanten under gammal och nyare tid. Ymer. Geografiska Annaler. 33 (3–4): 121–143. 90: 241–242. Östrem, G., 1959. Ice melting under a thin layer of —1973. Snow densities on Storglaciären in Spring and moraine, and the existence of ice cores in moraine summer. Geografiska Annaler. 54A (3–4): 155–158. ridges. Geografiska Annaler. 41: 228–230. —1973. Tarfala och dess forskningsverksamhet. Infor- —1961. A new approach to end moraine chronology. mation 1, STOU-NG, Naturgeografiska inst. Geografiska Annaler. 43 (3–4): 418–419. Stockholms universitet. 2:a uppl. 1975, 3:e uppl. —1962. Nya metoder för åldersbestämmning av 1978. 27 p. ändmoräner. Ymer 82: 241–252. —1973. Hydrologisk aktivitet inom undersöknings- —1962. Ice-cored moraines in Kebnekajse area. området Tarfala, (ur Vannet i Norden nr 1, s 12– Meddelande från Geografiska institutionen 29). Information 2, STOU-NG, Naturgeogr. inst., Stockholms univ. 154 p Stockholms universitet. 18 p. —1963. Comparative Crystallographic Studies on Ice —1979. Tarfala and it’s research activities. Naturgeo- from Ice-cored Moraines, Snow-banks and Glaciers. grafiska institutionen Stockholms universitet. Geografiska Annaler. 45 (4): 210–242. Forskningsrapportserien STOU-NG 34 (ISSN 0346- —1964. Ice-cored Moraines in Scandinavia. Geografiska 7406), 31 p. Annaler. 46 (3): 282–337. Schytt, V., Jonsson, S., and Cederstrand, P., 1963. Notes —1965. Problems of dating ice-cored moraines. on glaciological activities in Kebnekaise, Sweden – Geografiska Annaler. 47A (2): 1–38. 1963. Geografiska Annaler. 45 (4): 292–302. Östrem, G., Haakensen, N., and Melander, O., 1973. Smith, I. N. and Budd, W. F., 1979. The derivation of Atlas over breer i Nord-Skandinavia. Meddelande past climate changes from observed changes of gla- nr 46 från Naturgeografiska inst. Stockholms univ. ciers. Sea level, Ice, and Climatic Change (proceed- 315 p. ings of the Canbverra Symposium, Dec. 1979). IAHS 131: 31–52.

Doctor of Philosophy dissertations Cutler, P. M., 1996. Water input and subglacial tunnel evolution at Storglaciären, northern Sweden. PhD Bronge, C., 1989. Climatic Aspects of Hydrology and dissertation, Department of Geology and Geophys- Lake Sediments with Examples from Northern Scan- ics, University of Minnesota, xx pp. dinavia and Antarctica. Naturgeografiska Hock, R., 1998. Modelling of glacier melt and discharge. institutionen vid Stockholms universitet, Meddelande PhD dissertation, no 12430, Department of Geog- nr A 241 (ISBN 91-7146-785-8), 166 p. raphy, ETH Zurich, 126 pp. Brugger, K., 1992. A comperative study of the response Holmlund, P., 1988. Studies of the drainage and the re- of Rabots Glaciär and Storglaciären to recent cli- sponse to climatic change of Mikkaglaciären and mate change in Sweden, PhD dissertation, Depart- Storglaciären. Naturgeografiska institutionen vid ment of Geology and Geophysics, University of Min- Stockholms universitet. Meddelande nr A 220 (ISBN nesota, 287 p. 91-7146-590-1), 75 p. 40 Tarfala Research Station Annual Report 1997–98

Jansson, P., 1993. Interpretation of short-term varia- Kennett, M., 1987. An analysis of the scattering of ra- tions in ice dynamics, Storglaciären, Kebnekaise, dio waves within a temperate glacier. Department Northern Sweden. PhD dissertation, Department of of Physics, University of Bristol. 176 p. Geology and Geophysics University of Minnesota, Kohler, J. C., 1992. Glacial hydrology of Storglaciären, USA, Northern Sweden. PhD dissertation, Department of Jansson, P., 1994. Studies of short-term variations in ice Geology and Geophysics, University of Minnesota, dynamics, Storglaciären, northern Sweden. Natur- USA, 147 p. geografiska institutionen, Stockholms universitet, Pohjola, V. A., 1993. Ice Dynamical Studies on Avhandlingsserie (ISSN 1104-7208), Dissertation Storglaciären, Sweden. A study based on TV-video no.1 (ISBN 91-7153-247-1). observations of englacial Structures and deforma- Jonsson, S., 1970. Strukturstudier av subpolär glaciäris tion measurements within boreholes. Institutionen från Kebnekaiseområdet. Naturgeografiska institu- för geovetenskap vid Uppsala universitet. Acta uni- tionen, Stockholms universitet, Forskningsrapport- versitatis Upsaliensis, Comprehensive Summaries of serien 8, (ISSN 0346-7406),. 200p. Uppsala Dissertations from the Faculty of Science Karlén, W., 1976. Holocene climatic fluctuations indi- 470 (ISBN 91-554-3173-9). cated by glacier and tree-limit variations in north- Rapp, A., 1961. Studies of the postglacial development ern Sweden. Naturgeografiska institutionen, of mountain slopes. Geografiska institutionen vid Stockholms universitet. Forskningsrapportserien 23, Uppsala universitet. meddelande nr 159. (ISSN 0346-7406). Östrem, G., 1965. Studies of Ice-cored moraines. Natur- geografiska institutionen, Stockholms universitet, Esselte AB, Stockholm 1965.

Filosofie licenciatexamen, Master of Science Rosquist, G., 1989. Studies of glacier fluctuations and dissertations, or equivalent work, after 1980 climatic change. Naturgeografiska institutionen vid Stockholms universitet. Bronge, C., 1985. Hydrologisk verksamhet i Tarfala, Schneeberger, C., 1998. Glacier balance modeling using 1974-1982. En analys av bearbetningsmetoder och a GCM. Diploma thesis at the Institute of Geogra- resultat. Naturgeografiska institutionen, Stockholms phy, Department of Geology, Swiss Federal Institute universitet. Forkningsrapportserien STOU-NG 62, of Technology (ETH), Zurich. (ISSN 0346-7406), 81 p Schneider, C., 1992. GIS based modelling of the energy Goerke, U., 1993. Geologische untersuchungen im balance from Landsat-TM. Diplomarbeit at the De- südlichen Kebnekaise-gebiet, Tarfala, in den Skandi- partment of Physical Geography, University of navischen Kaledoniden, Nordschweden. Diplom- Freiburg, Germany. p. arbeit, Department of Geology / Paleontology, Schneider, T., 1994. Water movement and storage in the Ruprecht - Karls University, Heidelberg, Germany. firn of Storglaciären, northern Sweden. Diplomarbeit Hock, R., 1991. Aspects of the internal drainage system at the Department of Physical Geography, Univer- of Storglaciären, Sweden, as indicated by dye-trace sity of Freiburg, Germany. 74 p. studies. Diplomarbeit at the Department of Physical Schneider, T., 1998. Hydrological processes in the firn Geography, University of Freiburg, Germany. of Storglaciären. Naturgeografiska institutionen vid Jansson, E. P., 1992. Interpretation of short-term varia- Stockholms Universitet. tions in ice-dynamics, Storglaciären, Kebnekaise, Shimko, K. A., 1987. A study on structures in two val- northern Sweden. NGSU Research Report 89. ley glaciers in northern Sweden by observation and Krüger, G., 1985. Aktuelle Schneefleckenformung in den computer modelling. MS diss., Department of Geol- Skanden am beispiel des Kebnekaise (67o55’N, ogy and Geophysics, University of Minnesota, USA, 10o32’E), Nord-Lappland. Diplomarbeit im Fach Zimmerer, S., 1987. A study of the englacial and Geographie der matematisch-naturwissenschaftligen subglacial hydrology of Storglaciären, northern Facharbereiche der Georg-August-Universität Sweden. MS diss., Department of Geology and Geo- Göttingen. 55 p. physics, University of Minnesota, USA, Richardson, C., 1996. Klimatinriktade georadarstudier på glaciärer i svenska fjällen och på den antarktiska inlandsisen. Naturgeografiska institutionen vid Stockholms universitet.

Undergraduate papers (examensarbeten), Bomark, M., och Lundberg, C., 1995. GPS-mätning i after 1980 Tarfala 1994. Stomnät, metodförsök, amnslutning till RR92. Institutionen för Geodesi och Fotogram- Bodin, A., 1991. Kårsaglaciärens reträtt under 1900- metri, Kungliga Tekniska Högskolan, Stockholm. talet. Naturgeografiska institutionen vid Stockholms Examensarbete i Geodesi. 49 p. universitet, Examensarbete på geovetarlinjen, 24 p.

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Burman, H., och Rost. T., 1991. Uppmätning av ero- Lind, L., 1982. Studier av basal isrörelse på sion och sedimentation i Tarfaladalen med analytisk Isfallsglaciären, Kebnekaise, 1980-1981. Naturgeo- fotogrammetri. Institutionen för fotogrammetri, grafiska institutionen vid Lunds universitet. 47 p. Kungliga Tekniska Högskolan, Stockholm. Examens- Lindstrand, O., 1986. Sediment från Storglaciären, arbete i fotogrammetri nr 95, 37 p. Kebnekaise. En kvalitativ bestämning. Geologiska Calla, P., 1988. Datering av snökärnor borrade på institutionen vid Göteborgs universitet. 35 p. Grönlands inlandsis. Naturgeografiska institutionen Moberg, A., 1984. Massbalansundersökningar på vid Uppsala universitet. 24 p. Björlings glaciär, Kebnekaise, 1983. Naturgeogra- Eriksson, M., 1990. Storglaciärens bottentopografi fiska institutionen vid Stockholms universitet. 24 p. uppmätt genom radioekosondering. Naturgeogra- Neidhart, F., 1997. Die kartierung des Pårteglaciären fiska institutionen vid Stockholms universitet. 28 p. und die analyse seine veränderung von 1963 bis Finnander, M.-L., 1989. Vädrets betydelse för snöav- 1996. Fachhochschule Stuttgart - Hochschule für smältningen i Tarfaladalen. Naturgeografiska technik. Germany. institutionen vid Lunds universitet. 41 p. Näslund, J.-O., 1989. En studie av proglaciala lakustrina Fredin, O., 1997. Kortidsvariationer i isrörelse på sediment från Valfojaure, norra Sverige. Natur- Storglaciären. Naturgeografiska institutionen vid geografiska institutionen vid Stockholms universitet. Stockholms universitet. Examensarbete. 43 p. 14 p. Frisk, A. and Ståhl, L., 1985. Kalibrering av mätränna i Pettersson, R., 1996: Studier av isstrukturer och deras Tarfala. Kungliga Tekniska Högskolan, 42 p koppling till klimatet på två subpolära glaciärer i Hedin, M., 1984: Tarfalavagge - former och deglacia- Kebnekaise. Naturgeografiska institutionen vid tion. Naturgeografiska institutionen vid Stockholms Stockholms universitet. Examensarbete för filosofie universitet. 31 p. magisterexamen. 47 p. Hieltala, M., 1989. En utvärdering av areella Pohjola, V., 1986. Mätningar av hastighetsfördelningar, nederbördsmetoder och mätarplaceringar i Tarfala- längs en profil i Storglaciären, Kebnekaise, 1985. dalen. Naturgeografiska institutionen, Stockholms Naturgeografiska institutionen vid Uppsala universitet. 41 p. universitet. 34 p. Holmlund, P., 1982: Glaciärbrunnars genes och Richardson, C., 1993. Nischbildningsprocesser – En morfologi. Naturgeografiska institutionen vid fältstudie vid Passglaciären, Kebnekaise. Naturgeo- Stockholms universitet. 41 p. grafiska institutionen vid Lunds universitet, Huss, E., 1997. Glaciärfrontsreträtter under 1900-talet Seminarieuppsats nr 30, 58 p. - en detaljstudie av Räitaglaciärerna, norra Schneider, T., 1992. Suspended sediment transport in Lappland. Naturgeografiska institutionen vid the proglacial stream of Storglaciären, northern Stockholms universitet. Examensarbete för filosofie Sweden, 1980–1990. Avdelningen för hydrologi, kandidatexamen. 73 p. Uppsala universitet, C-uppsats, 27 p. Jansson, P., 1986. Variations in surface tilt on Strömberg, K., 1987. Vattentillskott till Storglaciären Storglaciären, Kebnekaise, Northern Sweden. Natur- från snösmältning på omgivande dalsidor. geografiska institutionen vid Stockholms universitet. Naturgeografiska institutionen vid Göteborgs 16 p. universitet. Karlöf, L., 1997. Densitetsutvecklingen i snö och firn Troëng, S., 1993. Glacialmorfologiska studier vid på Storglaciären under ett massbalansår kopplat till Pårtejekna, Sarek – en jämförelse mellan två vädrets förändringar. Naturgeografiska institutionen frontområden. Naturgeografiska institutionen vid vid Stockholms universitet. Examensarbete. Stockholms universitet. Examensarbete vid geovetar- Kjessel, R., 1986. Blöta lössnölaviner och slasklaviner. linjen, 27 p. Naturgeografiska institutionen vid Stockholms Wennberg, S., 1986. Nederbördsmätning i Tarfaladalen universitet. 56 p. - extremvärden och nederbördsfördelning. Natur- Klingbjer, P., 1996: Jökellopp vid Sälka. Naturgeo- geografiska institutionen vid Stockholms universitet. grafiska institutionen vid Stockholms universitet. 38 p. Examensarbete för filosofie magisterexamen. 56 p. Östling, M., 1986. Vattenbalansen i Storglaciären. Naturgeografiska institutionen vid Stockholms universitet. 31 p.

Compilations of data from Tarfala, (available Årsrapport 1988. Tarfala research station. Arjen at the department) Stroeven (ed.), 85 p. Årsrapport 1989. Tarfala research station. Arjen Bergman, V., 1988. Sommarnederbörd vid Tarfala- Stroeven and Mats Eriksson (eds). 76 p. stationen och i dess omgivningar 1965–1984. 39 p. Årsrapport 1990. Tarfala reserach station. Håkan Grudd Grudd, H., and Jansson, P., 1986. The 1984/85 mass and Axel Bodin (eds.), 96 p. balance of Storglaciären, Kebnekaise, Swedish Årsrapport 1990–1991. Tarfala research station. Håkan Lappland. 13p. Grudd (ed.), Forskningsrapportserien STOU-NG 92 Årsrapport från Tarfala forskningsstation, 1986. Peter (ISSN 0346-7406), 73 p. Jansson (ed.), 95 p. Årsrapport 1991–1992. Tarfala research station. Axel Årsrapport 1987. Tarfala research station. Gunhild Bodin (ed.), Forskningsrapportserien STOU-NG 96 Rosqvist (ed.), 103 p. (ISSN 0346-7406), 64 p.

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Tarfala Research Station Annual Report, 1992–93. Peter Tarfala Research Station Annual Report, 1995–96. Per Jansson, (ed.), NGSU Forskningsrapport 100. (ISSN Klingbjer, (ed.), NGSU Forskningsrapport 104. 0346-7406), 50 p. (ISSN 0346-7406), 76 p. Tarfala Research Station Annual Report, 1993–94. Peter Tarfala Research Station Annual Report, 1996–97. Per Jansson, (ed.), NGSU Forskningsrapport 102. (ISSN Klingbjer, (ed.), NGSU Forskningsrapport 105. 0346-7406), 66 p. (ISSN 0346-7406), 76 p. Tarfala Research Station Annual Report, 1994–95. Peter Tarfala Research Station Annual Report, 1997–98. Per Jansson, (ed.), NGSU Forskningsrapport 103. (ISSN Klingbjer, (ed.), NGSU Forskningsrapport 110. 0346-7406), 66 p. (ISSN 1403-9788), 50 p.

Publications in popular science Lundqvist, G., 1944. De svenska fjällens natur. STF:s förlag, Stockholm 1944. 440pp. Ahlmann, H. W:son, 1952. Kebnekajse. Svenska —1948. De svenska fjällens natur (2:nd edition). STF:s turistföreningens årsskrift 1952: 265–288. förlag, Stockholm 1948. 502 pp. Holmlund, P., 1986. Glaciärforskning i Tarfala. Till Karlén, W., och Holm, F., 1989. Glaciärerna smälter— Fjälls, Svenska Fjällklubbens årsskrift, 58: 48–53. istiden kommer ändå. Forskning och framsteg 1989 —1991. Valter Schytt och Tarfalastationen., Till Fjälls, (4): 4–11. Svenska Fjällklubbens årsskrift, 61-62: 48–53. Mannerfelt, C. M:son., 1940. I Kebnekaise. En —1992. Glaciärer och forskare i Tarfala under ett halvt Naturhistorisk rundvandring. Svenska turist- sekel. Geologklubben vid Stockholms universitet, föreningens årsskrift 1940: 312–338. Geologklubben 100 år, 61–67. Rosquist, G. and Karlén, W., 1996. Värmeböljor och —1995. Mikkaglaciären – dess liv, leverne och framtid. fimbulvintrar: klimatet de senaste 10 000 åren. Till Fjälls, Svenska Fjällklubbens årsskrift 65-66: 12– Jordens klimat. Naturvetenskapliga forskningsrådets 27. årsbok 1996, 97-105. Holmlund, P., och Schytt, A., 1989. Glaciärer—En Schytt, V., 1963. Glaciärernas liv. Svenska turist- kunskapsvandring på Storglaciären, Kebnekaise. föreningens årsskrift 1963: 144–158. Småskrift nr. 1 (ISBN 91-87636-01-8) från Ajtte —1963. Lapplands glaciärer. Natur i Lappland. Uppsala. museum. Jokkmokk 1989. 32 sidor. 158–171. —1995. Vi går mot en ny istid. Populär vetenskap 4: —1973. Glaciologiska metoder i klimatforskningens 34-39. tjänst. Svensk Naturvetenskap 1973. 14 p. —1995: Tarfala - Tarfalaverksamheten 50 år. En —1981. Det föränderliga klimatet. Här är vi hemma. jubileumsskrift med anledning av Tarfala- Rolf Edberg (ed.) Bra Böcker, 1982, 90–105. verksamhetens 50-årsjubileum. Stockholms universitet (ISBN: 91-7540-112-6), 48 s.

43 Tarfala Research Station Annual Report 1997–98 Boende på Tarfala Forskningsstation under 1998

Stationspersonal Per Holmlund Stationsföreståndare 38 Peter Jansson Forskarassistent 27 Krister Jonsson Tekniker 142 Mats Nilsson Tekniker 134

Extrapersonal Per Ekman Hantlangare 39 Johan Ekroth Hantlangare 55 Ulf Fastesson Hantlangare 27 Sara Runeborg Hantlangare 16 Hanna Falkeström Kock 22 Johan Norin Kock 96 Andrej Wigert Kock 22 Mart Nyman Amanuens 33

Projektansvariga och gästforskare Per-G Andreasson Uppsala Universitet 6 Prajukti Bhattucharaya Department of Geology and Geophysics, University of Minnesota, USA 23 Sven Blomkvist Institutionen för Systemekologi, Stockholms Universitet 4 Ian Brown Climate Impact Research Centre, Kiruna 6 Keith Brugger University of Minnesota, USA 2 Sara Frödin Naturgeografiska Institutionen, Stockholms Univeristet 46 Håkan Grudd Climate Impact Research Centre, Kiruna 4 Regine Hock Climate Impact Research Centre, Kiruna 51 Maria Johansson Climate Impact Research Centre, Kiruna 5 Per Klingbjer Naturgeografiska Institutionen, Stockholms Univeristet 12 David Morse University of Texas, USA 3 Jens Ove Näslund Naturgeografiska Institutionen, Stockholms Univeristet 20 Rickhard Pettersson Naturgeografiska Institutionen, Stockholms Univeristet 16 Cecilia Richardsson Naturgeografiska Institutionen, Stockholms Univeristet 17 Thomas Schneider Naturgeografiska Institutionen, Stockholms Univeristet 50

44 Tarfala Research Station Annual Report 1997–98

Wojceich Stankowskei Adam Mickiewicz Universit-Poznan, Polen 16 Leigh Sterns Carleton College in Northfield Minnesota, USA 30 Arjen Stroeven Kvartärgeologiska Institutionen, Stockholms Universitet 6 Erin Young University of Minnesota, USA 22

Kurser och grupper Akademiska hus, Luleå 14 Fältkurs, Artic Center, Rovaniemm, Finland 107 Gymnasieelever, Hjalmarlundbomsskolan i Kiruna 4 Mass Balance Workshop, IGS, arrangör Stockholms Universitet 93 MDC, Kiruna 30 NCC, Kiruna 4 Statens Fastighetsverk, Uppsala 4 Svenska Turistföreningen STF AB, Kebnekaise Fjällstation 395 Tarfalakursen, Naturgeografiska Institutionen, Stockholms Universitet 278 Tärendö Centralskola 33

Övriga Anna Schytt 20 Anna Nora Schytt 6 Personalgäster m m. 160

Totalt 1998 2138

45 Tarfala Research Station Annual Report 1997–98 Appendix 1

Snow depth survey - May 1998 and winter balance map 1997/98

7536000

580 510 510 610 545 410 412 325 545 470 420 450 380 330 Snow depths, May 1998 540 495 7535500 418 442 342 415 375 470 408 395 370 378 300 270 600 470 415 415 422 350 300 310 310 595 480 460 435 410 320 380 245 615 580 368 483 390 355 200 335 340 7535000 700 200 180 285 440 520 518 275 220 410 425 245 410 280 300 237 190 630 210 330 180 180 620 130 300 180 170 510 305 300 175 150 500 445 205 192 235 180 385 305 170 165 240 260 305 130 100 288 270 115 130 440 370 256 255 50 152 355 305 232 193 195 170 300 320 165 150 270 140 321 267 140 150 125 530 430 200 200 170 90 390 330 224 208 130 145 250 50 185 126 170 145 260 243 133 160 160 222 585 240 187 170 115 280 310 430 410 187 168 122 133 Northing (m) Northing 160 160 340 215 145 145 175 110 150 150 120 145 7534500 210 282 130 95 120 195 525 160 145 105 195 300 390 295 130 130 170 100 230 110 131 190 73 125 40 130 120 125 145 135 370 280 148 120 78 280 340 380 156 132 80 230 275 245 100 110 218 125 170 190 140 107 54 113 403 120 150 190 265 310 365 190 190 70 95 340 330 142 125 265 235 330 230 142 150 180 170 190 130 115 140 370 290 280 170 130 335 310 280 250 180 190 360 400 270 181 165 210 225 175 215 190 175 250 380 340 280 7534000 245 230 340

7533500 20000 21000 22000 23000 Easting (m)

7535800

7535600

7535400

7535200

7535000

7534800 Northing (m) Northing 7534600

7534400

7534200

7534000

20000 20200 20400 20600 20800 21000 21200 21400 21600 21800 22000 22200 22400 22600 22800 23000 23200 Easting (m)

46 Tarfala Research Station Annual Report 1997–98 Appendix 2

Stake locations 1998 and summer balance map 1997/98

7536000

31N8

29N6 27N6 31N5

7535000 27N2 16N314N2 12N3 10N2 28N1 26N1 18N2

Northing (m) 14 29 27 22N1 18N1 10N1 6N2 22 11N3 28S1 20 18 16 10 8N1 29S2 14S1 27S2 17S1 12N1 10S2 8 6 3 28S3 19S1 14S2 4N1 18S2 12 8S1 6S1 22S3 14S4 4S2 29S4 27S4 20S2 10S4 28S6 26S4 16S2 8S3 6S3 19S417S3 13S1 9S2

7534000

20000 21000 22000 23000 Easting (m)

7535800

7535600

7535400

7535200

7535000

7534800 Northing (m) Northing 7534600

7534400

7534200

7534000

20000 20200 20400 20600 20800 21000 21200 21400 21600 21800 22000 22200 22400 22600 22800 23000 23200 Easting (m)

47 Tarfala Research Station Annual Report 1997–98 Appendix 3

Stage-discharge relationship at Rännan 1986-1997 Data from 1986 from Bronge (1989)

Date h (m) Q (m3s-1) Date h (m) Q (m3s-1) Date h (m) Q (m3s-1)

1986 1.205 5.920 1986 1.210 4.742 1993 0.661 0.899 1986 1.245 6.062 1986 1.080 3.610 1993 0.689 1.060 1986 1.100 3.809 1986 0.930 2.612 1993 0.700 1.090 1986 1.120 4.524 1986 1.050 3.438 1993 0.714 1.260 1986 1.050 3.627 1986 0.960 2.710 1993 0.819 1.890 1986 1.100 4.299 1986 1.020 3.347 1993 0.920 2.670 1986 1.080 3.901 1986 1.050 3.300 1993 0.926 2.770 1986 0.860 2.346 1986 1.100 3.873 1993 1.093 4.420 1986 0.870 2.088 1986 0.460 0.635 1993 1.095 5.020 1986 0.850 2.324 1986 0.450 0.482 1993 1.239 6.810 1986 0.760 1.759 1986 0.430 0.417 96-07-22 0.989 4.208 1986 0.445 0.282 1986 0.430 0.200 96-07-25 1.060 5.104 1986 0.445 0.357 1986 0.890 2.028 96-07-25 1.061 5.099 1986 0.445 0.161 1986 0.925 2.044 96-07-28 1.034 4.803 1986 0.445 0.378 1986 1.055 3.255 96-07-28 1.048 4.957 1986 0.445 0.462 1986 1.060 3.724 96-08-20 1.417 10.070 1986 0.445 0.151 1986 1.135 3.645 96-08-21 1.670 16.814 1986 1.190 5.537 1986 1.135 3.988 96-08-21 1.612 14.520 1986 1.240 5.847 1986 1.150 4.815 96-08-21 1.507 12.181 1986 1.140 4.656 1986 0.925 2.198 97-07-08 1.246 6.457 1986 1.160 4.843 1986 0.760 1.455 97-07-08 1.286 6.840 1986 1.000 3.376 1986 0.480 0.512 97-07-12 1.006 4.201 1986 0.900 2.450 1986 0.480 0.339 97-07-12 1.026 4.252 1986 0.905 2.513 1993 0.467 0.362 97-07-17 1.071 4.502 1986 0.810 2.093 1993 0.570 0.436 97-07-17 1.074 4.562 1986 0.810 1.921 1993 0.603 0.618 97-07-17 1.146 4.577 1986 0.710 1.405 1993 0.620 0.717 97-08-22 1.088 4.674 1986 0.860 2.122 1993 0.661 0.912

Appendix 4

Stage-discharge relationship at Lillsjön 1993-1997

Date h (m) Q (m3s-1) Date h (m) Q (m3s-1) Date h (m) Q (m3s-1)

93-09-05 0.100 0.427 95-08-17 0.485 3.800 96-07-10 0.270 1.962 93-09-06 0.060 0.375 95-08-24 0.290 2.380 96-07-10 0.260 1.771 95-07-24 0.280 2.241 95-08-29 0.150 0.927 96-07-25 0.320 2.095 95-07-25 0.190 1.512 95-08-29 0.150 0.875 97-07-08 0.438 3.078 95-07-28 0.400 3.000 95-09-01 0.117 0.647 97-07-12 0.315 2.411 95-08-04 0.350 2.796 96-07-02 0.132 0.819 97-07-17 0.388 2.753 95-08-16 0.380 3.091 96-07-04 0.223 1.541 97-07-25 0.280 1.900 95-08-17 0.408 2.880 96-07-08 0.288 2.232

48 Tarfala Research Station Annual Report 1997–98 Appendix 5

Mean daily discharge at Rännan 1997. Digits in italics are probably to high, due to ice damming at the gauge station

Date h (m) Q (m3s-1) Date h (m) Q (m3s-1) Date h (m) Q (m3s-1) Date h (m)Q (m3s-1)

1/6 1/7 0.97 3.187 1/8 0.97 3.197 1/9 1.15 5.299 2/6 2/7 0.97 3.187 2/8 0.98 3.287 2/9 1.10 4.590 3/6 3/7 0.99 3.390 3/8 1.02 3.723 3/9 1.12 4.956 4/6 4/7 1.13 5.010 4/8 0.99 3.380 4/9 1.14 5.229 5/6 5/7 1.23 6.550 5/8 1.07 4.304 5/9 1.18 5.716 6/6 6/7 1.16 5.454 6/8 1.14 5.201 6/9 1.09 4.577 7/6 0.20 0.025 7/7 1.12 4.956 7/8 1.14 5.146 7/9 1.01 3.591 8/6 0.45 0.313 8/7 1.19 5.955 8/8 1.17 5.555 8/9 0.94 2.878 9/6 0.59 0.695 9/7 1.17 5.541 9/8 1.23 6.534 9/9 0.97 3.137 10/6 0.71 1.247 10/7 1.06 4.112 10/8 1.12 4.876 10/9 0.88 2.396 11/6 0.67 1.037 11/7 1.00 3.506 11/8 0.92 2.723 11/9 0.81 1.838 12/6 0.58 0.680 12/7 1.03 3.812 12/8 0.81 1.831 12/9 0.78 1.607 13/6 0.57 0.632 13/7 1.08 4.439 13/8 0.72 1.296 13/9 0.94 2.916 14/6 0.68 1.085 14/7 1.10 4.590 14/8 0.65 0.942 14/9 1.02 3.646 15/6 0.73 1.351 15/7 1.09 4.565 15/8 0.63 0.840 15/9 0.87 2.291 16/6 0.73 1.351 16/7 1.09 4.527 16/8 0.68 1.071 16/9 0.79 1.671 17/6 0.65 0.960 17/7 1.10 4.641 17/8 0.76 1.526 17/9 0.75 1.449 18/6 0.63 0.857 18/7 1.10 4.654 18/8 1.06 4.171 18/9 0.71 1.242 19/6 0.76 1.526 19/7 1.07 4.316 19/8 1.08 4.390 19/9 0.68 1.085 20/6 1.28 7.374 20/7 1.12 4.889 20/8 0.97 3.177 20/9 0.65 0.924 21/6 1.19 5.910 21/7 1.06 4.135 21/8 1.09 4.489 21/9 0.63 0.840 22/6 1.15 5.271 22/7 1.01 3.602 22/8 1.20 6.001 22/9 0.60 0.739 23/6 1.07 4.255 23/7 1.00 3.506 23/8 1.34 8.533 23/9 0.58 0.653 24/6 0.95 3.011 24/7 0.99 3.359 24/8 1.18 5.745 24/9 0.68 1.090 25/6 0.87 2.275 25/7 0.97 3.127 25/8 1.09 4.514 25/9 0.99 3.359 26/6 0.73 1.323 26/7 1.03 3.801 26/8 1.01 3.538 26/9 0.90 2.539 27/6 0.61 0.784 27/7 1.03 3.789 27/8 1.06 4.147 27/9 0.79 1.690 28/6 0.60 0.754 28/7 1.00 3.516 28/8 0.97 3.157 28/9 0.75 1.449 29/6 0.76 1.508 29/7 1.01 3.559 29/8 1.03 3.857 29/9 0.73 1.351 30/6 0.90 2.488 30/7 1.07 4.316 30/8 1.09 4.527 30/9 0.69 1.144 31/7 1.04 3.880 31/8 1.16 5.497

49 Tarfala Research Station Annual Report 1997–98 Appendix 6

Mean daily discharge at Rännan 1998. Digits in italics are probably to high, due to ice damming at the gauge station

Date h (m) Q (m3s-1) Date h (m) Q (m3s-1) Date h (m) Q (m3s-1) Date h (m)Q (m3s-1)

1/6 0.16 0.014 1/7 1.14 5.201 1/8 1.19 5.895 1/9 0.76 1.490 2/6 0.16 0.014 2/7 1.14 5.187 2/8 1.14 5.201 2/9 0.73 1.351 3/6 0.17 0.015 3/7 1.07 4.328 3/8 1.06 4.171 3/9 0.73 1.346 4/6 0.18 0.020 4/7 0.97 3.127 4/8 1.04 3.880 4/9 0.74 1.391 5/6 0.19 0.023 5/7 0.90 2.556 5/8 1.08 4.414 5/9 0.72 1.301 6/6 0.20 0.028 6/7 0.98 3.267 6/8 1.11 4.823 6/9 0.72 1.263 7/6 0.21 0.029 7/7 1.04 3.971 7/8 1.06 4.123 7/9 0.72 1.263 8/6 0.20 0.028 8/7 1.09 4.577 8/8 1.01 3.548 8/9 0.83 1.964 9/6 0.24 0.043 9/7 1.15 5.369 9/8 1.01 3.559 9/9 0.89 2.404 10/6 0.24 0.046 10/7 1.35 8.727 10/8 0.96 3.059 10/9 0.95 2.934 11/6 0.24 0.046 11/7 1.32 8.059 11/8 0.93 2.786 11/9 1.00 3.453 12/6 0.30 0.086 12/7 1.45 10.814 12/8 0.86 2.228 12/9 0.87 2.291 13/6 0.35 0.139 13/7 1.76 19.497 13/8 0.87 2.315 13/9 0.76 1.520 14/6 0.42 0.254 14/7 1.54 13.007 14/8 0.83 2.008 14/9 0.84 2.045 15/6 0.49 0.387 15/7 1.67 16.659 15/8 0.91 2.582 15/9 0.79 1.690 16/6 0.49 0.409 16/7 1.47 11.273 16/8 1.10 4.641 16/9 0.72 1.296 17/6 0.58 0.649 17/7 1.31 7.985 17/8 1.23 6.550 17/9 0.67 1.033 18/6 0.67 1.047 18/7 1.18 5.716 18/8 1.20 6.031 18/9 0.63 0.844 19/6 0.67 1.023 19/7 1.17 5.541 19/8 1.15 5.341 19/9 0.60 0.739 20/6 0.72 1.301 20/7 1.51 12.107 20/8 1.01 3.602 20/9 0.92 2.723 21/6 0.87 2.275 21/7 1.36 8.865 21/8 1.00 3.453 21/9 1.24 6.746 22/6 1.29 7.533 22/7 1.19 5.865 22/8 1.25 6.779 22/9 0.99 3.349 23/6 1.27 7.201 23/7 1.19 5.955 23/8 1.15 5.327 23/9 0.81 1.838 24/6 1.18 5.701 24/7 1.17 5.541 24/8 1.16 5.440 24/9 0.71 1.211 25/6 1.10 4.641 25/7 1.17 5.672 25/8 0.99 3.359 25/9 0.65 0.920 26/6 0.97 3.207 26/7 1.14 5.174 26/8 0.93 2.768 26/9 0.60 0.731 27/6 0.98 3.277 27/7 1.12 4.956 27/8 0.91 2.625 27/9 0.56 0.599 28/6 1.06 4.112 28/7 1.13 4.996 28/8 0.89 2.413 28/9 29/6 1.13 4.983 29/7 1.07 4.231 29/8 0.89 2.429 29/9 30/6 1.16 5.454 30/7 1.12 4.876 30/8 0.88 2.396 30/9 31/7 1.35 8.629 31/8 0.80 1.783

50 Department of Physical Geography, Stockholm University

Research Report Series

Series editor: Peter Jansson

110. Klingbjer, P. (Ed.) 1999: Tarfala Research Station 87. Isaksson, E., 1992: Spatial and temporal patterns in Annual Report 1997–98. (50 p.) snow accumulation and oxygen isotopes, Western 109. Allard, A., Ihse, M., Nordberg, M.-L., 1998: Dronning Maud Land, Antarctica. (86 s.) Vegetationsförändringar i fjällen. (64 s.) 86. Skånes, H., 1991: Förändringar i odlingslandskapet 108. Löfvenhaft, K., Ihse, M., 1998: Biologisk mångfald och dess konsekvenser för gräsmarksfloran. En och fysisk planering. (112 s.) studie från södra Halland. (70 s.) 107. Eknert, B., 1998: Biotopernas betydelse för fågelfau- 85. Ihse, M., Löfgren, T., 1991: Bestämning av biomassa nan i odlingslandskapet. (58 s.) på rikkärr i norra Finland med hjälp av spektral- 106. Moberg, A. (Ed.) 1998: Modelling in Physical mätning. (58 s.) Geography. Projects Works 1998. (89 p.) 84. Isaksson, P-O., 1991: Vittringsstudier på 105. Klingbjer, P. (Ed.) 1998: Tarfala Research Station Nordaustlandet. (24 s.) Annual Report 1996–97. (76 p.) 83. Näslund, J-O., Pohjola, V., Stroeven, A., 1991: 104. Klingbjer, P. (Ed.) 1997: Tarfala Research Station Glaciological surveys in Vestfjella and Annual Report 1995–96. (76 p.) Heimefrontfjella, Dronning Maud Land, 103. Jansson, P. (Ed.) 1996: Tarfala Research Station Antarctica, 1998/1990. (71 s.) Annual Report 1994–95. (66 p.) 82. Forsberg, P., 1991: Lichenometriska studier av laven 102. Jansson, P. (Ed.) 1995: Tarfala Research Station Aspicilia Calcarea på norra Gotland. (31 s.) Annual Report 1993–94. (66 p.) 81. Runborg, S., 1990: Tomteby – Vegetations- 101. Forsberg, P., 1995: Geomorfologiska studier av förändringar i ett ålderdomligt odlingslandskap i kustplattformen utmed Gotlands nordvästra en öländsk by, studerade genom flygbildstolking. klintkust. (74 p.) (61 s.) 100. Jansson, P. (Ed.) 1994: Tarfala Research Station 80. Syrén, P., 1990: Reflektans för fysiska modeller av Annual Report 1992–93. (50 p.) skogsbestånd som funktion av belysningsgeometri. 99. Schneider, T., 1994: Water movement and storage in (33 s.) the firn of Storglaciären, Northern Sweden. (89 p.) 79. Granath, L., 1990: Radarsynkron ekolodning - Ett 98. Näslund, J-O, Bodin, A., 1994: Studies on ice nytt system för batymetrisk kartläggning och dynamics, mass balance and paleoclimate in East bottenmaterialundersökning. (36 s.) Antarctica 1991–92. (43 p.) 78. Granath, L., 1989: Kartläggning av erosionskänsliga 97. Bodin, A., 1993: Physical properties of Kårsa stränder längs Rödkobbsleden. (30 s.) Glacier in Swedish Lapland. (24 p.) 77. Sadeghi-Nad, A., 1989: Computer aided analysis of 96. Bodin, A. (red.), 1993: Årsrapport, Tarfala Research Landsat MSS data for mapping urban/suburban Station. (63 s.) land use and land cover in Teheran area, IRAN. 95. Eriksson, M.G., Björnsson, J., Herzfeld, U.C., (42 s.) Holmlund, P., 1993: The bottom Topography of 76. Bronge, C., 1989: Holocene climatic fluctuations Storglaciären. A new map based on old and new recorded from lake sediments in Nicholson Lake, ice depth measurements, analyzed with Vestfold Hills, Antarctica. (23 p.) geostatistical mehods. (48 s.) 75. Kleman, J., & Alm, G., 1989: Estimation of the 94. Schneider, T., Bronge, C., 1992: Discharge and atmospheric influence on a Landsat TM scene suspended sediment transport of the proglacial using low-altitude radiometer data. (28 p.) stream of Storglaciären, Northern Sweden, 1980– 74. Bronge, C., 1989: The hydrology of proglacial 1990. (44 s.) Chelnok Lake, Vestfold Hills, Antarctica. (41 p.) 93. Nordberg, M-L, 1992: Mapping of local-scale 73. Holmlund, P., Isaksson, I., Karlén, W., 1989: thermal variations in Landsat images for risk Massbalans, isrörelse och isdynamik – preliminära assessment of forest regeneration failures. (105 s.) resultat från fältsäsongen 1988/89 i Vestfjella och 92. Grudd, H. (red.), 1992: Årsrapport, Tarfala Re- heimefrontfjella, V. Dronning Maud Land, search Station. (73 s.) Antarktis. (66 p.) 91. Rosqvist, G., 1992: Late Holocene glacial activity 72. Bronge, C., Openshaw, A., 1989: New instrument recorded in lacustrine sediments on El Altar, for measuring water discharge by the salt dillution Ecuador. (27 s.) method. (12 p.) 90. Rosqvist, G., 1992: Late quaternary glacial and 71. Österholm, H., 1988: The glacial history of Prins climatic history of the Ecuadorian Andes. (11 s.) Oscars Land, Nordaustlandet, Svalbard. (3 p.) 89. Jansson, E.P., 1992: Interpretation of short-term 70. Österholm, H., 1988: The glacial striation on Prins variations in ice dynamics, Storglaciären, Oscars Land, Nordaustlandet, Svalbard. (10 p.) Kebnekaise, Northern Sweden. (83 s.) 69. Österholm, H., 1988: Raised beaches and crustal 88. Holmgren, K., 1992: The late Quaternary climate in uplift on Prins Oscars Land, Svalbard. (20 p.) Botswana. A litterature review. (30 s.)