Acta geographica Slovenica, 60-2, 2020, 141–153
THE GEOCHEMISTRY OF ICE IN THE
SOUTHEASTERN ALPS, SLOVENIA
Anne Carey, Devin Smith, Susan Welch, Matija Zorn, Jure Tičar,
Matej Lipar, Blaž Komac, Berry Lyons
Cave ice in the Ivačičeva Cave in the Julian Alps (southeastern Alps, Slovenia).
JAKA ORTAR, ZRC SAZU AnTOn MeliK GeOGRAphiCAl inSTiTUTe ARChive

Carey et al., The geochemistry of ice in the southeastern Alps, Slovenia
DOI: https://doi.org/10.3986/AGS.7420
UDC: 911.2:551.324(234.323.6)
551.324:550.4(234.323.6)
COBISS: 1.01
Anne Carey
1
, Devin Smith
2
, Susan Welch
1
, Matija Zorn
3
, Jure Tičar
3
, Matej Lipar
3
, Blaž Komac
3
,
Berry Lyons
1
The geochemistry of ice in the southeastern Alps, Slovenia
ABSTRACT: The Triglav Glacier in the Julian Alps and the Skuta Glacier in the Kamnik-Savinja Alps are
among the south-easternmost glaciers in the Alps. Historical data show that ice masses are undergoing mass
loss as the overall climate warms. Glacier ice and cave ice contain a wealth of paleoclimatic information,
and rapid sampling is needed if any such information is to be saved before the ice is completely melted.
We present the first comprehensive geochemical and water isotope data from glacier ice, meltwater, spring
water, and cave ice in the Mount Triglav area and glacier ice from the Skuta Glacier. The samples primarily
reflect the initial precipitation signal that has been greatly modified by the input of local CaCO
3
-rich dust
with lesser amounts of marine aerosol and vegetation debris.
KEY WORDS: glaciochemistry, glaciokarst, ice caves, cave ice, water isotope, Triglav Glacier, Skuta Glacier,
Alps
Geokemija ledu v jugovzhodnih Alpah, Slovenija
POVZETEK: Triglavski ledenik v Julijskih Alpah in Ledenik pod Skuto v Kamniško-Savinjskih Alpah sta
med najbolj jugovzhodnimi ledeniki v Alpah. Njuno dolgoletno opazovanje kaže, da se ledenika zaradi
segrevanja ozračja krčita. Ker ledeniški in jamski led hranita številne podatke o preteklem podnebju, je
njuno vzorčenje nujno, dokler so podatki (led) še na razpolago. V članku predstavljamo prve obsežnejše
podatke o geokemiji in vodnih izotopih iz ledeniškega ledu, talilne vode, izvirske vode in jamskega ledu
na območju Triglava ter ledeniškega ledu iz Ledenika pod Skuto. Vzorci v prvi vrsti odražajo začetni signal
padavin, ki je bil močno spremenjen z vnosom aerosola, obogatenega s karbonatom ter v manjši meri z
delci morskega in rastlinskega izvora.
KLJUČNE BESEDE: geokemija, glaciokras, ledene jame, jamski led, vodni izotopi, Triglavski ledenik, Ledenik
pod Skuto, Alpe
The paper was submitted for publication on January 17
th
, 2019.
Uredništvo je prejelo prispevek 17. januarja 2019.
142
1
The Ohio State University, School of Earth Sciences, Byrd Polar and Climate Research Center,
Columbus, Ohio, USA
carey.145@osu.edu (https://orcid.org/0000-0002-0272-5254), welch.318@osu.edu, lyons.142@osu.edu
(https://orcid.org/0000-0002-3143-7251)
2
The Ohio State University, School of Earth Sciences, Columbus, Ohio, USA
smith.11880@osu.edu (https://orcid.org/0000-0001-6945-7306)
3
Research Centre of the Slovenian Academy of Sciences and Arts, Anton Melik Geographical Institute,
Ljubljana, Slovenia
matija.zorn@zrc-sazu.si (https://orcid.org/0000-0002-5788-018X), 
jure.ticar@zrc-sazu.si (https://orcid.org/0000-0003-3567-8084),
matej.lipar@zrc-sazu.si (https://orcid.org/0000-0003-4414-0147),
blaz.komac@zrc-sazu.si (https://orcid.org/0000-0003-4205-5790)

1 Introduction
The Triglav Glacier in the Julian Alps (NW Slovenia) at app. 2450–2550 m and the Skuta Glacier in the
Kamnik-Savinja Alps (N Slovenia) at app. 2000–2200 m are the only glacier remains in Slovenia (Gabrovec
et al. 2013; 2014; Triglav Čekada et al. 2020; Triglav Čekada and Zorn 2020; Figure 1) and among the south-
easternmost glaciers in the Alps (Grunewald and Scheithauer 2010). Due to their small size and the
relief-dependent lack of movement, they are defined as glacierets (Kumar 2011). As such, from the envi-
ronmental perspective they represent important mountain geomorphosites (Reynard and Coratza 2016).
The beginning of the research of the Slovenian Alps dates back to the 17
th
and 18
th
century (Mikša
and Zorn 2016), and the size of the Triglav Glacier has been estimated as far back in time as 1897 (Triglav
Čekada, Zorn and Colucci 2014; Del Gobbo et al. 2016). Excellent historical data on the Triglav and Skuta
glaciers are available due to continuous detailed measurements of both glaciers by the ZRC SAZU Anton
Melik Geographical Institute since 1946 and 1948, respectively (Pavšek 2004; 2007; Gabrovec et al. 2013;
2014). Between the years 2000 and 2013 the ice volume of the Triglav Glacier has decreased from 35,000 m
3
to app. 7,400 m
3
(Del Gobbo et al. 2016) and has probably reached the smallest size since the Last Glacial
Maximum (Lipar et al. 2021). The Skuta Glacier has also experienced mass loss during the past six to seven
decades (Pavšek 2007; Triglav Čekada et al. 2020).
Glacier ice and cave ice represent a wealth of paleoclimatic information (Y ao et al. 2011), but work in
Slovenia (Mihevc 2018) and in other parts of the Julian Alps (Colucci et al. 2016) indicates that, like the
Triglav and Skuta glaciers, these ice masses continue to undergo mass loss as the overall climate warms.
Rapid sampling of these deposits is needed if any such information is to be preserved. In this paper we
present the first comprehensive geochemical and water isotope data, collected in 2017 and 2018, from both
ice and meltwater from Triglav and Skuta glaciers’ areas. These data also include measurements of cave
ice from the Ivačičeva Cave (IC; Figures 2 and 4) and the Triglav Shaft (TS; Figures 3 and 4) located very
close to the Triglav Glacier, and water from the spring of the Triglavska Bistrica Creek (TBC) in the Vrata
Valley below the Triglav Glacier (TG) at 1175 m (Figure 1). The purpose of this work was to describe the
chemistry of the ice and its meltwater and to provide new information on the isotopic composition at this
elevation in the Julian Alps and the Kamnik-Savinja Alps. We also continue to evaluate the potential for
use of cave ice in paleoclimatological studies (Carey et al. 2019). In addition, we discuss the hydrological
connectivity among precipitation (i.e., glacier ice), meltwater, cave ice and karst spring water in glaciokarst
landscape (Zorn, Hrvatin and Perko 2020).
2 Study area and methods
2.1 Study area
The Mount Triglav (2864 m; Julian Alps) regional landscape has been termed glaciokarst (Kunaver 1983;
Žebre and Stepišnik 2015) with the flatter depressions in the landscape providing locations for the col-
lection and accumulation of winter snow (Del Gobbo et al. 2016). The ice samples from the Triglav Glacier
(TG) area come from the glacier, the Triglav Shaft (TS; Triglavsko brezno) and Ivačičeva Cave (IC; Ivačičeva
jama). The Triglav Shaft is a vertical ice cave 274 m deep. Entrance to the cave occurs at 2377 m and was cov-
ered by the glacier until the early 20
th
century. The Ivačičeva Cave is situated next to the Kredarica mountain
hut at 2457m (Tičar et al. 2018). The spring water sample is from spring of the Triglavska Bistrica Creek (TBC)
in the Vrata Valley which is app. 1200 m directly below the Triglav Glacier and Triglav Shaft (Figure 1).
The Julian Alps bedrock is dominated by Triassic-Jurassic shallow water carbonate rocks (Šmuc and
Rožič 2009). There is a weather observatory at 2514 m that is less than 0.5 km from the glacier. The mean
annual temperature during 1981–2010 was –1.0 ± 0.6 °C and the mean annual precipitation was 2070 mm
(water equivalent), with mean winter snow accumulation of 5.14 m (Del Gobbo et al. 2016). The wind
Acta geographica Slovenica, 60-2, 2020
143
Figure 1: Map showing location of sampling location and the extent of the Triglav Glacier since 1850. Inset map shows location of larger, detailed
figure.p p. 144

Carey et al., The geochemistry of ice in the southeastern Alps, Slovenia
144
Valentin Stanič Hut
2332 m
Kredarica Hut
2515 m
Content by: Blaž Komac, Matej Lipar, Jure Tičar, Matija Zorn
Map by: Manca Volk Bahun
Source: GIAM 2017, GURS 2018
© 2020, ZRC SAZU Anton Melik Geographical Institute
0 250 500 m
S L O V E N I A
C R O A T I A
HUNGARY
A U S T R I A
ITALY
Triglav
Glacier
Skuta Glacier
Triglav
2864 m
Glava
2426 m
Mali Triglav
2738 m
Kredarica
2539 m
Vrh Snežne konte
2362 m
Rž
2538 m
Begunjski vrh
2460 m
Triglav Sha#
2377 m
Ivačičeva Cave
2457 m
Triglavska Bistrica
Triglavska Bistrica Spring
1175 m
0 30 60 km
Legend
Sampling location
2018
Triglav Glacier in years:
1850
1946

Acta geographica Slovenica, 60-2, 2020
145
Figure 2: Ice sampling in the Ivačičeva Cave.
Figure 3: Entrance chamber of the Triglav Shaft where ice samples were taken.
M A T IJ A Z o R N J U R E T IČ A R Figure 4: Sketch of the entrance part of the Triglav Shaft and the Ivačičeva Cave with the location of sampling (black dot).p p. 146

Carey et al., The geochemistry of ice in the southeastern Alps, Slovenia
146
0 m
10 m
20 m
30 m
40 m
50 m
Vertical profile
Pool of water
Entrance 2
Ivačičeva Cave
(2457 m a.s.l.)
Entrance 1
Entrance 1
Entrance 2
Vertical profile
Pool of water
Triglav Shaft
(2377 m a.s.l.)
Entrance 1
Pool of water
Vertical profile
Continuation
of the cave
Entrance 2
Side view Side view
Plan view
J U R E T IČ A R

Acta geographica Slovenica, 60-2, 2020
147
direction is influenced by the top of Mt. Triglav just west from the station, thus the prevailing winds come
from northwest or southeast with speeds up to 190 km/h (Nadbath 2014).
Ice was also sampled from the Skuta Glacier (SG; Figure 1). The Skuta Glacier (Kamnik-Savinja Alps)
is located in a cirque oriented toward the northwest, which preserves it from the Sun for most of the year
and also influences the wind direction. The glacier lies at an average elevation of app. 2070 m. The broad-
er Mt. Skuta (2532 m) area is dominated by Triassic carbonate rocks (Mioč 1983), so the setting of the glacier
is also in a karstic environment. Both glaciers are fed with snow also through avalanches.
2.2 Methods
Ice samples were collected using a clean ice axe, placed into plastic bags and allowed to melt. Samples for
ion analysis were filtered in the laboratory through 0.45 µ m pore size Millipore filters using clean plastic
syringes into precleaned low density polyethylene bottles, as discussed in Carey et al. (2019). Samples for
water isotope analyses were not filtered but immediately upon complete melting of the ice, the resultant
water was decanted into scintillation vials, minimizing any headspace. Water samples were collected direct-
ly into precleaned polyethylene bottles and filtered (except the isotope samples) using the same technique
as the melted ice.
The samples were kept in the dark in a refrigerator until shipped to the laboratory at The Ohio State
University. Major ions were analyzed by ICP-OES (Inductively Coupled Plasma Optical Emission
Spectrometry) and ion chromatographic techniques (Welch et al. 2010). Nutrients (NO
2
–
+ NO
3
–
, NH
4
+
,
PO
4
3–
and H
4
SiO
4
) were determined with a Skalar SAN++ nutrient analyzer using methods supplied by
the manufacturer. The δ
18
O and δD of water were analyzed using a Picarro liquid water isotope analyzer.
Samples were compared to VSMOW (δ
18
O=0‰; δ
2
H=0‰) and to internal laboratory standards as a means
of correcting raw data. Some of the ice collection bags were filled with our cleanest deionized water and
analyzed as samples to provide any evidence of contamination from the bags and these were used as blanks.
Chloride, sulfate, sodium and potassium in these blanks were below our levels of detection while mag-
nesium and calcium concentrations had mean values of 0.9 µ M and 3.5 µ M, respectively. Details on accuracy
and precision can be found in Welch et al. (2010) and Carey et al. (2019). Bicarbonate concentrations were
determined by the difference in charge balance as HCO
3
–
= Σcations – Σanions as discussed in Welch et
al. (2010).
3 Results
The major ion and nutrient data are presented in Table 1. Several general statements can be made about
the data. They include, in general, Ca>>Mg=Na>K; HCO
3
>SO
4
>Cl; ΣDIN (sum of NO
2
–
+ NO
3
–
+
NH
4
+
)>>PO
4
3–
; except for the Triglavska Bistrica Spring (TBC) in the Vrata Valley, H
4
SiO
4
concentrations
are very low. The δ
18
O and δD range between –8.1‰ and –12.7‰ and between –56.3‰ and –96.4‰, respec-
tively (Table 2). We have plotted our isotopic analyses of the ice with a regional meteoric water line which
we developed from published data (Figure 5). The isotope values all fall on or very close to the regional
meteoric water line. The very high Ca and HCO
3
values strongly indicate that all the ice and snow are great-
ly influenced by local CaCO
3
-rich dust.
4 Discussion
4.1 Geochemical data
The mean values for both the glacier and cave ice in the Triglav Glacier area (Table 2) are compared to
a high elevation snow pit and ice core data from Mt. Ortles, Italy (Gabrielli et al. 2010) and the closest ice
core to the Triglav Glacier as the Mt. Ortles core is the only core taken from the Eastern Alps, near the
border of Italy, Switzerland and Austria. These samples from Italy were collected at an elevation of 3860 m
and is the nearest high-elevation ice data adjacent to ice-free areas. These ice data represent a regional pic-
ture of high elevation precipitation chemistry in this area of the Alps and it is the nearest ice core analyzed

Carey et al., The geochemistry of ice in the southeastern Alps, Slovenia
148
Table 1: Major ion and nutrient chemistry of ice and water samples.
Sample Sample Cl
–
SO
4
2–
HCO
3
–
Na
+
K
+
Mg
2+
Ca
2+
SDIN PO
4
3–
Si N:P
number µ M µ M µ M µ M µ M µ M µ M µ M µ M µ M
TS 1 Cave Ice 3.9 9.3 248.3 3.9 3.1 4.5 127 12.0 0.50 1.1 24.1
TS 2 Cave Ice 1.7 6.8 234 2.6 0.5 2.1 121 0.4 0.24 0.7 1.7
TS 3 Cave Ice 2.0 15.8 406.5 5.7 2.0 4.9 212 1.7 0.15 2.6 11.3
TS 4 Cave Ice 3.4 9.1 243.5 5.7 1.3 4.5 127 5.1 0.09 0.9 56.7
TS 5 Cave Ice 3.4 14.2 337.5 7.0 1.5 6.2 179 10.0 0.02 1.0 333
TS 6 Cave Ice 1.7 11.1 828.5 2.2 <0.3 4.1 171 10.5 0.03 1.2 16.7
TG 1 Glacier Ice 9.3 9.0 281.2 8.3 8.9 4.1 143 23.9 0.12 1.1 199
TG 2 Melt water 1.1 7.2 182.3 0.9 <0.3 4.1 96 3.6 0.05 0.6 72.0
TG 3 Melt water 0.8 10.1 315.5 0.9 <0.3 6.6 163 3.7 0.04 0.9 92.5
TBC Spring Water 4.5 3.9 1223 0.4 <0.3 134 496 24.9 0.04 6.2 622
SG 1 Glacier Ice 11.2 16.8 315 3.5 1.8 <4 179 3.9 <0.01 0.5 >390
SG 2 Glacier Ice 1.8 16.7 92.6 10.9 1.5 6.2 52 1.6 <0.01 0.3 >160
IC 1 Cave Ice 2.1 8.4 4.52 1.81 22.4 200 5.9 0.07 0.3 84.3
IC 2 Cave Ice 1.4 9.8 2.25 0.83 2.98 121 1.4 0.04 0.1 35.0
IC 3 Cave Ice 2.0 7.4 2.71 0.94 5.48 109 2.9 0.03 0.1 96.7
IC 4 Cave Ice 0.9 3.4 3.28 0.47 1.86 77 1.7 0.03 <0.1 56.7
IC 4 - test Cave Ice 1.5 5.8 1.84 0.63 3.74 124 3.3 0.03 <0.1 110
IC 5 Cave Ice 1.8 7.4 2.37 5.13 26.3 134 16.4 0.03 0.1 547

for some of the same analyzed in our samples. We assume that the precipitation regime in the Triglav region
is generally similar to that in the Mt. Ortles area and it is then modified, either by the input of chemicals
as the precipitation falls or after it is deposited on the glacier surface. Enrichment factors (Triglav ice/Mt.
Ortles snow) can then be computed for elements under investigation (Table 1). These enrichment factors
range from as little as 1.1 for Mg and as high as 19.1 for Ca (Table 3). Calcium in the Mt. Ortles snow has
been shown to be a proxy for »dust« (Gabrielli et al. 2010). Because the surrounding bedrock in the Triglav
area is carbonate, we assume that these very large enrichments of Ca in the Triglav ice and in the melt-
water are both due to the local input of CaCO
3
-rich dust. The dust either dissolves as the ice melts or is
solubilized when acid is added to the cation samples prior to ICP-OES analysis, or both. The lesser enrich-
ments in Cl, SO
4
, Na, and K are probably also related to increased particle input from marine aerosol,
pollution, and/or organic matter debris deposited as primary precipitation or blown onto the glacier sur-
face as aeolian deposition through time. The very low H
4
SiO
4
values suggest, however, that the deposited
dust either is extremely low in silicate minerals or that these minerals are filtered out of the sample dur-
ing processing. We have observed debris on the filter paper after filtration so the latter is more likely. This
phenomenon of local dust deposition onto glacier surfaces has been observed on many glaciers all over
the world, including on glaciers in the ice-free regions of Antarctica where local soils can be suspended
and re-deposited by winds (Lyons et al. 2002; 2020). In addition, local dust deposition and erosion com-
monly occur in Slovenia, even in lower-lying regions (e.g., Zorn 2009; Miler 2014; Miler and Gosar 2015;
Zupančič, Horvat and Skobe 2015).
The cave ice has a geochemistry similar to the meltwater, which may suggest that the cave ice is formed
from the refreezing of summer glacier melt (Table 1).
DIN concentrations have mean value of 6.3 μM and median of only 3.3 μM. All but two of the sam-
ples have DIN < 1 μM. The DIN values observed in the Ivačičeva Cave ice are lower than the average DIN
in ice of 15 μM and 24 μM observed respectively in Paradana Cave and Snežna Cave, two other ice caves
in Slovenia studied (Carey et al. 2019). The similar values observed in the Triglav area glacier ice of 6.5 μM
Acta geographica Slovenica, 60-2, 2020
149
Table 2: Stable isotope analyses of ice and water samples compared to VSMOW (δ
18
O=0‰; δ
2
H=0‰).
Sample Sample Values Accuracy
number
δ
18
O, ‰ δD, ‰ δ
18
O, ‰ δD, ‰
TS 1 Cave Ice –12.10 –87.44 0.08 1.51
TS 2 Cave Ice –11.38 –77.05 0.08 1.51
TS 3 Cave Ice –9.64 –65.40 0.08 1.51
TS 4 Cave Ice –10.53 –72.54 0.08 1.51
TS 5 Cave Ice –11.96 –82.15 0.08 1.51
TS 6 Cave Ice –10.67 –79.79 0.08 1.51
TG 1 Glacier Ice –10.08 –68.63 0.08 1.51
TG 2 Melt water –8.06 –52.72 0.08 1.51
TG 3 Melt water –8.15 –52.37 0.08 1.51
TBC Spring Water –9.84 –64.94 0.08 1.51
SG 1 Glacier Ice –8.69 –58.06 0.08 1.22
SG 2 Glacier Ice –8.90 –58.72 0.08 1.22
IC 1 Cave Ice –8.82 –57.46 0.05 0.59
IC 2 Cave Ice –8.63 –57.04 0.05 0.59
IC 3 Cave Ice –8.40 –54.16 0.05 0.59
IC 4 Cave Ice –8.54 –56.14 0.05 0.59
IC 4 - test Cave Ice –9.01 –59.90 0.05 0.59
IC 5 Cave Ice –8.12 –53.75 0.05 0.59

Carey et al., The geochemistry of ice in the southeastern Alps, Slovenia
and the cave ice of 6.3 μM suggest that the DIN mass flux behaves conservatively in the glaciokarst flow
systems in the Triglav area. The dissolved PO
4
3–
concentrations were at or below 0.50 μM in all the sam-
ples with the majority of samples measuring < 0.1 μM, with very low values in the Skuta Glacier ice and
in the cave ice (Table 1).
The DIN:P molar ratios varied widely, from app. 2 to 390 in the ice to a ratio of 622 in the spring water
(Table 1). The glacier melt yielded DIN:P of 72 and 92.5, higher than those of aquatic vegetation (app. 16)
but lower than DIN:P for trees of app. 165 (Sterner and Elser 2002). It is not clear what these large variations
of dissolved N:P ratios mean or if they truly reflect any biogeochemical significance. The low PO
4
3–
con-
centrations reflect its particle reactivity (and removal during the filtration step), and the presence of oxidizing
conditions in all of these milieux.
4.2 Isotopic data
As noted above, the δ
18
O and δD values fall close to the regional meteoric water line, suggesting little to
no evaporation, sublimation, nor transpiration has occurred (Figure 5). The two glacier ice δ
18
O samples
had values of –8.9‰ and –8.7‰, while the glacier melt water was lighter, at –10.08‰. The Triglav Shaft
ice had a greater range of δ
18
O, –12.10‰ to –9.64‰ which may suggest a seasonal variation of snow and
water input. This pattern may also represent even longer time variations than seasonal ones, as we do not
know the true age of this material. However, the melt and spring waters are generally more enriched than
the glacier ice values. Whether this enrichment is due to some evaporitic loss or melt actually being gen-
erated from ice (or more recent snow) with a heavier isotopic signature cannot be determined.
The cave ice samples show little variation in δ
18
O, similar to what has been observed in the Snežna
Cave ice app. 70 km to the east of the Triglav Glacier (Carey et al. 2019). This observation suggests that
the ice from which we obtained samples may have originated from one water mass or from a constant or
nearly constant isotopic source, as has been suggested previously for the Snežna Cave (Carey et al. 2019).
The unusual environmental setting of high elevation karst has allowed these ice caves to exist in a cold-
er climate but continued warming (Hrvatin and Zorn 2017; 2018) will drive the loss of this part of the
terrestrial cryosphere and perhaps the loss of the paleoclimate information contained therein. In addition,
the terrestrial cryosphere will continue to transform in underground karst cryosphere, so the monitoring
of the process is of essential.
5 Conclusion
We have sampled glacier ice, meltwater, spring water, and cave ice in the Triglav Glacier area and on the
Skuta Glacier in the southeastern Alps (Slovenia) and analyzed these materials for major cations and anions,
nutrients, and water stable isotopes. The samples primarily reflect the initial precipitation signal that has
been greatly modified by the input of local CaCO
3
-rich dust with lesser amounts of marine aerosol and
vegetation debris. There is surprisingly little variation between the glacier ice and meltwater in their major
elemental composition. The H
4
SiO
4
also varies little, indicating the lack of silicate mineral weathering in
those environments. The dissolved PO
4
3–
concentrations are very low while the DIN concentrations vary
by more than an order of magnitude. This produces DIN:P ratios that also vary greatly and thus limit our
150
Table 3: Comparison of mean chemistry from Triglav Glacier samples with Mt. Ortles snow pit chemistry (Gabrielli et al. 2010). Enrichment factors
are calculated as Triglav Glacier chemistry divided by that of the Mt. Ortles snow pit.
Mean values Cl SO
4
Na K Mg Ca
µM µM µM µM µM µM
Mt. Ortles snow pit at 3860 m 2.4 2.1 1.9 0.4 4.2 7.7
Mean Triglav Glacier 4.3 12.0 5.5 2.3 4.5 145
Mean Ivačičeva Cave ice 1.6 7.0
Triglav Glacier enrichment factor 1.8 5.7 2.9 5.7 1.1 19.1

ability to evaluate the sources of and the ecological impacts of these nutrients within this environment.
The δ
18
O and δD values of the sample fall very close to the regional meteoric water line indicating very
little modification of the primary precipitation by other processes, such as evaporation. The rapid loss of glac-
ier ice, as documented by the on-going work of personnel from the ZRC SAZU Anton Melik Geographic
Institute (e.g., Gabrovec 2013; 2014), and also the loss of cave ice, as documented by Mihevc (2018) and
others (Colucci et al. 2016), suggest strongly that in this region of the southeastern Alps the cryosphere
is rapidly being lost due to climate warming and the increasing summer temperatures will undoubtedly
hasten the loss.
ACKNOWLEDGEMENTS: We are very grateful for the support from The Ohio State University’s Slovene
Research Initiative that supported the collaboration of Anne E. Carey and W . Berry Lyons with Matija Zorn,
Blaž Komac, Jure Tičar, and Matej Lipar. Partial support came from research program no. P6-0101 and
infrastructure programme no. I0-0031 of the Slovenian Research Agency.
6 References
Carey, A. E., Zorn, M., T ičar, J., Lipar, M., Komac, B., W elch, S. A., Smith, D. F ., Lyons, W . B. 2019: Glaciochemistry
of Cave Ice: Paradana and Snežna Caves, Slovenia. Geosciences 9-2. DOI: https://doi.org/10.3390/
geosciences9020094 
Colucci, R. R., Fontana, D., Forte, E., Potleca, M., Guglielmin, M. 2016: Response of ice caves to weather
extremes in the southeastern Alps, Europe. Geomorphology 261. DOI: https://doi.org/10.1016/
j.geomorph.2016.02.017
Acta geographica Slovenica, 60-2, 2020
151
–30
–14 –13 –12 –11 –10 –9 –8 –7
–40
–50
–60
–70
–80
–90
–100
–110
δD(‰)
δ (‰)
18
O
TS 1
TS 6
TG 1
TS 3
SG 2
SG 1
IC 4
IC 3
IC 5
TG 2 TG 3
IC 2
IC 1
TBC
TS 4
TS 2
TS 5
IC 4– test
Figure 5: Triglav glacier area samples collected during 2017–2018. Also plotted is the regional meteoric water line for Slovenia of δD=7.94*δ
18
O+9.029
(regional line developed by Carey et al. 2019). Samples used to calculate the regional meteoric water line were collected at Global Network for Isotopes
in Precipitation (GNIP) sites: Ljubljana (336 samples from 1981–2010), Portorož (84 samples from 2000–2006), and Kozina (39 samples from 2000–2003)
(from data of Vreča et al. 2006; 2014). All GNIP data are available at the website of the International Atomic Energy Agency (Internet 1).

Carey et al., The geochemistry of ice in the southeastern Alps, Slovenia
Del Gobbo, C., Colucci, R. R., Forte, E., Triglav Čekada, M., Zorn, M. 2016: The Triglav Glacier (South-
Eastern Alps, Slovenia): volume estimation, internal characterization and 2000–2013 temporal evolution
by means of ground penetrating radar measurements. Pure and Applied Geophysics 173-8. DOI:
https://doi.org/10.1007/s00024-016-1348-2
Gabrielli, P ., Carturan, L., Gabrieli, J., Dinale, R., Krainer, K., Hausmann, H., Davis, M., Zagorodnov, V .,
Seppi, R., Barbante, C., Dalla Fontana, G., Thompson, L. G. 2010: Atmospheric warming threatens the
untapped glacial archive of Ortles mountain, South Tyrol. Journal of Glaciology 56-199. DOI:
https://doi.org/10.3189/002214310794457263
Gabrovec, M., Hrvatin, M., Komac, B., Ortar, J., Pavšek, M., Topole, M., Triglav Čekada, M., Zorn, M. 2014:
Triglavski ledenik. Geografija Slovenije 30. Ljubljana. DOI: https://doi.org/10.3986/9789610503644
Gabrovec, M., Ortar, J., Pavšek, M., Zorn, M., Triglav Čekada, M. 2013: The Triglav Glacier between the
years 1999 and 2012. Acta geographica Slovenica 53-2. DOI: https://doi.org/10.3986/AGS53202
Grunewald, K., Scheithauer, J. 2010: Europe’s southernmost glaciers: response and adaptation to climate
change. Journal of Glaciology 56-195. DOI: https://doi.org/10.3189/002214310791190947
Hrvatin, M., Zorn, M. 2017: Trendi pretokov rek v slovenskih Alpah med letoma 1961 in 2010. Geografski
vestnik 89-2. DOI: https://doi.org/10.3986/GV89201
Hrvatin, M., Zorn, M. 2018: Recentne spremembe rečnih pretokov in pretočnih režimov v Julijskih Alpah.
Triglav 240. Ljubljana. DOI: https://doi.org/10.3986/9789610500841
Internet 1: https://nucleus.iaea.org/wiser/index.aspx (9. 9. 2019).
Kumar, R. 2011: Glacieret. Encyclopedia of Snow, Ice and Glaciers. Dordrecht. DOI: https:/ /doi.org/10.1007/
978-90-481-2642-2_203
Kunaver, J. 1983: Geomorfološki razvoj Kaninskega pogorja. Geografski zbornik 22.
Lipar, M., Martín-Pérez, A., Tičar, J., Pavšek, M., Gabrovec, M., Hrvatin, M., Komac, B., Zorn, M., Zupan
Hajna, N., Zhao, J.-X., Drysdale, R. N., Ferk, M. 2021; Subglacial carbonate deposits as a potential proxy
for a glacier's former presence. The Cryosphere 15. DOI: https://doi.org/10.5194/tc-15-17-2021
Lyons, B., Foley, K., Carey, A., Diaz, M., Bowen, G., Cerling, T. 2020: The isotopic geochemistry of CaCO
3
encrustations in Taylor Valley, Antarctica: Implications for their origin. Acta geographica Slovenica
60-2. DOI: https://doi.org/10.3986/AGS.7233
Lyons, W . B., Nezat, C. A., Benson, L. V ., Bullen, T. D., Graham, E. Y ., Kidd, J., Welch, K. A., Thomas, J.
M. 2002: Strontium isotopic signatures of the streams and lakes of Taylor Valley, southern Victoria Land,
Antarctica: Chemical weathering in a polar climate. Aquatic Chemistry 8. DOI: https:/ /doi.org/10.1023/
A:1021339622515
Mihevc, A. 2018: Ice caves in Slovenia. Ice Caves. Amsterdam. DOI: https://doi.org/10.1016/B978-0-12-
811739-2.00030-9
Mikša, P ., Zorn, M. 2016: The beginnings of the research of Slovenian Alps. Geografski vestnik 88-2. DOI:
https://doi.org/10.3986/GV88206 
Miler, M. 2014: SEM/EDS characterisation of dusty deposits in precipitation and assessment of their origin.
Geologija 57-1. DOI: https://doi.org/10.5474/geologija.2014.001 
Miler, M., Gosar, M. 2015: Chemical and morphological characteristics of solid metal-bearing phases
deposited in snow and stream sediment as indicators of their origin. Environmental Science and Pollution
Research International 22. DOI: https://doi.org/10.1007/s11356-014-3589-x
Mioč, P . 1983: Osnovna geološka karta SFRJ 1 : 100.000, tolmač lista Ravne na Koroškem. Zvezni geološki
zavod. Beograd.
Nadbath, M. 2014: Meteorološka postaja Kredarica. Naše okolje 21-8.
Pavšek, M. 2004: Ledenik pod Skuto: ledeniški dragulj na senčni strani Kamniško-Savinjskih Alp.
Geografski obzornik 51-3.
Pavšek, M. 2007: Ledenik pod Skuto kot pokazatelj podnebnih sprememb v slovenskem delu Alp. Dela
28. DOI: https://doi.org/10.4312/dela.28.207-219
Reynard, E., Coratza, P . 2016: The importance of mountain geomorphosites for environmental education:
examples from the Italian Dolomites and the Swiss Alps. Acta geographica Slovenica 56-2. DOI:
https://doi.org/10.3986/AGS.1684
Sterner, R. W , Elser, J. J. 2002: Ecological Stoichiometry: Biology of Elements from Molecules to the Biosphere.
Princeton.
152

Šmuc, A., Rožič, G. 2009: Tectonic geomorphology of the Triglav Lakes Valley (easternmost Southern Alps,
NW Slovenia). Geomorphology 103-4. DOI: https://doi.org/10.1016/j.geomorph.2008.08.005
Tičar, J., Lipar, M., Zorn, M., Kozamernik, E. 2018: Triglavsko podzemlje. Triglav 240. Ljubljana. DOI:
https://doi.org/10.3986/9789610500841
Triglav Čekada, M., Barbo, P ., Pavšek, M., Zorn, M. 2020: Changes in the Skuta Glacier (southeastern Alps)
assessed using non-metric images. Acta geographica Slovenica 60-2. DOI: https://doi.org/10.3986/
AGS.7674
Triglav Čekada, M., Zorn, M. 2020: Thickness and geodetic mass balance changes for the Triglav Glacier
(southeastern Alps) from 1952 to 2016. Acta geographica Slovenica 60-2. DOI: https:/ /doi.org/10.3986/
AGS.7673
Triglav Čekada, M., Zorn, M., Colucci R. R. 2014: Changes in the area of the Canin (Italy) and Triglav
glaciers (Slovenia) since 1893 based on archive images and aerial laser scanning. Geodetski vestnik
58-2. DOI: https://doi.org/10.15292/geodetski-vestnik.2014.02.274-313
Vreča, P ., Krajcar Bronić, I., Horvatinčić, N., Barešić, J. 2006. Isotopic characteristics of precipitation in
Slovenia and Croatia: Comparison of continental and maritime stations. Journal of Hydrology 330,
3-4. DOI: https://doi.org/10.1016/j.jhydrol.2006.04.005
Vreča, P ., Krajcar Bronić, I., Leis, A., Demšar, M. 2014: Isotopic composition of precipitation at the GNIP
station Ljubljana (Reaktor), Slovenia – period 2007–2010. Geologija 57-2. DOI: https:/ /doi.org/10.5474/
geologija.2014.019
Welch, K. A., Lyons, W . B., Whisner, C., Gardner, C. B., Gooseff, M. N., McKnight, D. M., Priscu, J. C. 2010:
Spatial variations in the geochemistry of glacial meltwater streams in the Taylor Valley, Antarctica.
Antarctic Science 22-6. DOI: https://doi.org/10.1017/S0954102010000702
Y ao, T ., Liu, Y ., Zhao, H., Y u, W . 2011: Geochemistry of snow and ice. Encyclopedia of Snow, Ice and Glaciers.
Dordrecht. DOI: https://doi.org/10.1007/978-90-481-2642-2_176
Zorn, M. 2009: Erosion processes in Slovene Istria – part 1: Soil erosion. Acta geographica Slovenica 49-1.
DOI: https://doi.org/10.3986/AGS49102
Zorn, M., Hrvatin, M., Perko, D. 2020: Hydrological connectivity: an introduction to the concept. Geografski
vestnik 92-1. DOI: https://doi.org/10.3986/GV92102
Zupančič, N., Horvat, A., Skobe, S. 2015: Environmental impact of dusting from the Koper port bulk cargo
terminal on the agricultural soils. Acta geographica Slovenica 55-1. DOI: https:/ /doi.org/10.3986/AGS.826
Žebre, M., Stepišnik, U. 2015: Glaciokarst landforms and processes of the southern Dinaric Alps. Earth
Surface Processes and Landforms 40-11. DOI: https://doi.org/10.1002/ESP .3731
Acta geographica Slovenica, 60-2, 2020
153