Alterations of the nitrogen mineralization rates in soils of forest community depending on the ski...
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Journal of Mountain Science (Bimonthly, Started in 2004)
http://jms.imde.ac.cn
Volume 8 Number 1 February 2011
Contents
1–9 CUI Peng, HU Kaiheng, ZHUANG Jianqi, YANG Yu
Debris Flow Discharge Calculation and Inundation Simulation 10–23 Jieh-Jiuh WANG, Hoe I. LING
Developing a Risk Assessment Model for Typhoon-triggered Debris Flows 24–36 Marina SKRYPNIKOVA, Olga USPENSKAYA, Olga KHOKHLOVA
Paleoclimate Study of Mountain Ecosystems by Multiple Group Biological Analysis 37–45 Kalantari N., Alizadeh B., Mohammadi A.R., Keshavarzi. M.R.
A hydrochemical and Dye- tracing Investigation in the Posht-e-Naz Karstic Aquifer, Alburz Mountain,
Northern Iran 46–52 HAN Fang, YANG Zhaoping, LIU Xinyu, DI Feng
Impact Assessment and Protection of Outstanding Landscape Integrity in a Natural Heritage Site: Fairy
Valley, Kanas Nature Reserve, Xinjiang, China 53–61 Gürcan GÜLERYÜZ, Serap KIRMIZI, Hülya ARSLAN, Ece KONDU YAKUT
Alterations of the Nitrogen Mineralization Rates in Soils of Forest Community Depending on the Ski Run
Construction (Mount Uludağ, Bursa, Turkey) 62-74 Abhishek CHANDRA, P. Pardha SARADHI, R.K.MAIKHURI, K.G.SAXENA, K.S. RAO
Traditional Agrodiversity Management: A Case Study of Central Himalayan Village Ecosystem 75–86 Yadav UPRETY, Ram C. POUDEL, Hugo ASSELIN, Emmanuel K. BOON, Krishna K. SHRESTHA
Stakeholder Perspectives on Use, Trade, and Conservation of Medicinal Plants in the Rasuwa District of
Central Nepal 87–95 Chandra Prakash KALA, Rakesh Kumar MAIKHURI
Mitigating People-Park Conflicts on Resource Use through Ecotourism: A Case of the Nanda Devi
Biosphere Reserve, Indian Himalaya 96–102 WU Yong, HE Siming, LUO Yu, LI Xinpo
Failure Mechanisms of Post-Earthquake Bedrock Landslides in Response to Rainfall Infiltration 103–107 YOU Yong, PAN Huali, LIU Jinfeng, OU Guoqiang
The Optimal Cross-section Design of the “Trapezoid-V” Shaped Drainage Canal of Viscous Debris Flow
Serial parameters: CN51-1668/P*2004*B*A4*107*en*p*25* *11*2011-02
J. Mt. Sci. (2011) 8: 53–61 DOI: 10.1007/s11629-011-1127-6
Alterations of the Nitrogen Mineralization Rates in Soils of
Forest Community Depending on the Ski Run Construction
(Mount Uludağ, Bursa, Turkey)1)
Gürcan GÜLERYÜZ1*, Serap KIRMIZI2, Hülya ARSLAN1, Ece KONDU YAKUT1
1 Uludağ University, Faculty of Science and Arts, Department of Biology, 16059 Görükle/Bursa Turkey
2 Uludağ University, Gemlik Asım Kocabıyık Graduate Vocational School, 16600 Gemlik/Bursa Turkey
* Correspondence author, e-mail: [email protected]; Tel: +902242941788; Fax: +902242941899
© Science Press and Institute of Mountain Hazards and Environment, CAS and Springer-Verlag Berlin Heidelberg 2011
Abstract: Since 1940s, Mount Uludağ (Bithynian Olympus) has been considered famous with winter sports center in Turkey. In addition, it is one of the rare places because of its plant diversity and is also one of the important plant areas of Turkey. The ski run constructions are rapidly increased in the past decades in the alpine and subalpine belts of the mountain. Rate of nitrogen mineralization and some properties of soil were investigated in the soils of the three ski runs and undisturbed neighborhood forest sites. These ski runs are at the upper part of the forest belt in the mountain. Abies bornmuelleriana forest community is the postclimax and very sensitive to destruction. The rates of the nitrogen mineralization in the soils were determined in controlled conditions (60% water-holding capacity, 20°C). Nitrification and nitrogen mineralization were in the ski run inside where the natural recovery started, increased compared with the outside of the ski runs. Water-holding capacity, organic carbon, and total nitrogen were decreased in the massive damaged ski run, and due to these changes, the rates of mineralization and nitrification were also decreased. Keywords: Sub-alpine; Abies bornmuelleriana
forest; Ski run; Disturbance; Nitrogen mineralization; Nitrification
Introduction
Mountain ecosystems have harsh climatic conditions, and they are sensitive and susceptible to disturbances in soils (Chapin and Körner 1995, Ellenberg 1988, Körner 1999, Wipf et al. 2005). The quality of soil in managed mountain ecosystems changes depending on climate, soil conditions and land use (Sanchez-Maranon et al. 2002). Alpine and/or subalpine ecosystems are affected by machine grading of ski runs, recreational activities, and use of artificial snow. The machine grading applications in the ski runs remove or heavily damage the upper layers of soil and the vegetation (Bayfield 1996, Titus 1999, Ruth-Balaganskaya and Myllynen-Malinen 2000, Urbanska and Fattorini 2000, Wipfet al. 2005).
1) A part of this study represented by Ece Kondu Yakutas her MSc Thesis in Graduate School of Natural andApplied Sciences, University of Uludağ, Bursa, Turkeyin 2006.
Received: 9 December 2009 Accepted: 23 July 2010
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The recovery of disturbed alpine sites, where short growing seasons, shallow soils, and cool temperatures limit revegetation success, proceed at best very slowly and often does not occur completely if topsoil has been destroyed (Titus 1999, Urbanska 1995, Urbanska and Fattorini 2000). The process of machine grading accelerates erosion and, consequently, the reduction in depth of surface organic matter, increase in soil bulk density, and reduction in infiltration rates: the biodiversity may also be damaged (Marion and Merriam 1985, Urbanska 1995, Marion and Cole 1996, Hammit and Cole 1998, Titus 1999, Ruth-Balaganskaya and Myllynen-Malinen 2000). The alterations of physical and chemical properties directly and indirectly affect the microbial communities and processes, nutrient status, and water-holding capacity (WHC) of the soil (Lal and Stewart 1992, Zabinski and Gannon 1997). Soil properties, such as pH and organic matter, nitrogen, carbon contents, C/N ratio, and WHC are closely associated with the decomposition rates of organic matter (Runge 1983). The revegetation of the soil with native plants is required to decrease the velocity of erosion (Munshower 1994). The vegetation recovery lowers the source of disturbance and supports the functional plant and soil interaction system in the long term (Gross et al 2004).
Nitrogen mineralization (Nmin) is an important factor of ecosystem productivity because available N limits plant growth in many terrestrial systems (Runge 1983, Vitousek and Howarth 1991). For this reason, the N mineralization rate is used to show N availability associated with field productivity and plant development (Keeney 1980). Nitrogen mineralization, which is regulated by soil properties, such as content of soil organic matter; microbial biomass and activity; and temperature, pH, and moisture of the soil, is a common indicator of soil quality (Runge 1983, Knoepp et al. 2000) and has proved useful to assess ecosystem dynamics (Rehder 1994). The N mineralization rate in soil can be determined by field incubation (in situ) or under controlled laboratory conditions (Knoepp et al. 2000). Changes in litter quality lead to changes in N mineralization rates (Hassink 1994, Steltzer and Bowman 1998). Land-use changes have a strong influence on the N balance of ecosystems. For example, Vitousek et al. (1979)
reported that forest clearance may lead to elevated N loss through denitrification and leaching of nitrate. Güleryüz et al (2008) reported that N mineralization rate is high in soils of ruderal communities on disturbed sites in the sub-alpine belt of Uludağ Mountain and varies with dominant species and, a difference in net N mineralization rate can be attributed to organic C, total N and moisture content of soils.
Mount Uludağ is the highest mountain in the Marmara region including Thrace and the northwestern side of the Anatolian peninsula. The climate of the mountain changes from the base to the summit and causes a rich “plant diversity”. Due to its natural plant communities and various geomorphologic structures an area of 11,338 ha was established as a National Park in 1961, and then, this area was enlarged up to 12,762 ha in 1998. However, Uludağ is also an important winter tourism center in Turkey since 1940s. In the Uludağ winter sports center, the secondary vegetation grows on some ski runs by natural processes; however, in some other ski runs, the surface is disturbed by erosion. The Abies bornmuelleriana forest community has been destroyed for ski run construction in Uludağ. Güleryüz et al (2010), in their previous study of these ski slopes, determined that the values of soil parameters [WHC, total nitrogen, organic carbon and calcium, magnesium and potassium contents] were depressed in proportion to the disturbance level. However, they reported that the soil parameters were less degraded when secondary vegetation was growing on the disturbed areas. This study aimed to determine N mineralization rates and some soil properties of the ski slopes and undisturbed neighborhood forest sites and to show the adverse effects of land disturbance.
1 Material and Methods
1.1 Study area
Uludağ Mountain is located at 40°04' N and 29°13' E. The construction of ski runs increased in Uludağ in the last decade. These activities concentrated around the western ski runs between 1700 and 2150 m. Environmental problems arising from winter tourism activities and other facilities in
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the mountain have been determined through vegetation mapping studies previously (Güleryüz et al. 1998, Arslan et al. 1999, Arslan et al. 2004). Soils from three disturbed ski runs, in Mount Uludağ sub-alpine belt and Abies bornmuelleriana forest community representing the outside of the ski runs were chosen as research sites. The research area is on the 1900-2000 m altitude. The ski runs are on the northern and eastern parts of the Fatin hill, and above the timberline on Mount Uludağ. The main rock of the soil is granite and the land has 15-20 % slope. Abies bornmuelleriana forest community forms the natural plant cover on the mentioned sites of the hill, where there are ski runs. The plant cover decreases to 30 % on the north, and increases to 100 % on eastern part of the hill. Fagus orientalis grows as an accompanying species in the forest community on the east, whereas the dwarf shrubs, Juniperus communis and Vaccinnium myrtillus become dominant in the sub-plant cover. Nomenclature follows the Flora of Turkey and the East Aegean Islands (Davis 1965-1985).
Ski Run I was first established in 1968 by a government unit and was loaned to a private institution. The inside of the ski run has been consecutively under construction for a long time. The plant cover at the outer forest site is approximately 40-50 %.
Ski Run II was constructed in 1968, which has almost 80 % plant cover. It has no disturbance for a long time, therefore, Festuca cyllenica has become dominant and Juniperus communis, Vaccinnium myrtillus, and Genista lydia grow as accompanying species. The forest cover bounding the ski run can reach up to 60-80 %.
Ski Run III, established in 1991, is the youngest among the ski runs, the plant cover has a ruderal character and has Verbascum olympicum as the dominating species, and the accompanying species are Carduus olympicus, Thymus bornmuelleri, Anthemis cretica, Urtica dioica, and Lolium perenne. The plant cover in the outside forest is 100 %.
1.2 Sampling, experiments, and analyses
Three replicates of soil samples from each ski run (I, II, and III) and from their neighborhood forest sites (undisturbed) were taken. Samples
were taken from three different places at each sample site with a 15×15×15 cm steel frame in July 2001; soil samples were taken from two layers (0-5 and 5-15 cm). Soils were sieved through a 4-cm sieve, total soil weight was then determined, and 200-300 g samples were kept for analyses. Soil samples were air-dried and kept in paper bags in the laboratory for analysis.
The WHC of the soil samples was calculated using the differences between the fresh and dry weights of materials, which were saturated and then dried at 80°C until a constant weight was obtained. Soil samples (100 g) were put into polyethylene bags, and were moistened with distilled water until the WHC was 60 %. These bags prevent escape of mineral N and water (and moisture) but permit the exchange of CO2 and O2. The moistened samples were put into an incubator and were kept at 20°C in dark conditions for 9 weeks (63 days).
The mineral N of the soil was determined by a microdistillation method (Bremner and Keeney 1965). Mineral N (NH4+-N and NO3--N) was analyzed three times during the 63 days of incubation: at the beginning of incubation period, on the 21st and on the 63rd day. Net mineral N accumulations were calculated for 21 days (mg Nmin
/100 g dry soil/21 days) and 42 days (mg Nmin /100 g dry soil /42 days). Differences between these values were used to calculate the net mineral N production for each period.
Total N in soil was determined by a Kjeldahl wet digestion method using salicylic-sulfuric acid and selenium (Steubing 1965). The contents of CaCO3 (%) and organic C (%) in soil were determined by the Scheibler method and wet incineration method (digestion with concentrated sulfuric acid and titration by K2Cr2O7), respectively (Steubing 1965). The pH of air-dried soil samples was measured with a soil: water ratio of 1:2.5 (in saturated paste).
The differences among the sampling sites regarding to the net mineralization yield were tested by analysis of variance. Significant differences between groups were determined using the Tukey’s Honest Significant Difference (HSD) test (Zar 1984). The simple correlation between net mineral N productivity at the end of 63 days (mg Nmin /100 g dry soil / 63 days) and some soil factors (N, C, C/N ratio, pH and WHC) were tested as well.
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Table 1 The comparison of some properties at the sampling sites in the three ski runs of the Mount Uludağ sub-alpine belt. [Different letters indicate significant differences amongst the groups according to Tukey HSD test (α=0.05). Mean ± Standard Deviation (n = 3)].
All of the tests were performed at the significant level of α=0.05, with the Statistica Ver 6.0 (StatSoft Inc., Tulsa USA, 1984-1995) program.
2 Results and Discussion
Some soil characteristics of the sampling sites are given in Table 1. The significant differences among the sampling sites were found for soil total N, organic C, C/N ratio, maximum WHC, and pH (p<0.05). Soil pH was generally lower in the forest than in the ski runs (Table 1). The outside of the ski runs is naturally covered by Abies bornmuelleriana forest, and the soil has acidic character due to both granite substratum and soil organic matter content. The soil pH was increased for the inner part of the ski runs I and II. The highest soil pH was determined in the inside of ski run I, which was the most disturbed ski run and could also be explained with the continuing construction activities.
Massive soil destruction has negative effects on plant growth, and it causes decreases in soil N content as well (Munshower 1994). The massive destruction can cause decrease in plant cover, lower the thickness of organic matter layer, cause
losses in the topsoil layer, increase in bulk density, and decrease the infiltration rates (Lal and Stewart 1992, Zabisnki and Gannon 1997). Similar results were found during the preparation studies for ski run construction from different parts of the world (Urbanska 1995, Titus 1999, Ruth-Balaganskaya and Myllynen-Malinen 2000). The disturbance inside the ski runs I and III caused important losses of N. For example, although total N % content was 0.05 in the inside of ski run I, it was 0.30 % for the outside of ski run III and inside of the ski run II (Table 1). The primary production of terrestrial ecosystems has been affected by the factors such as species diversity and distribution and N capital and/or status (Chapin 1980, Wedin and Tilman 1990, Olff et al. 1994). Normally, the expected N capital is approximately 1000 kg N/ha in mild conditions, the highest value was 715 kg N/ha in our research area (Table 1) even in 0-5 cm layer of undisturbed (II-outside) places. Nitrogen stocks were lowered to 217 kg N/ha (I-inside) with disturbance. The effect of the destruction of plant cover on C content was also significant (Table 1). For example, the percentage of C content was 0.9 for the inside of the ski run I and 3.0 for the outside of the ski run I. The relative decrease was
Sampling Sites Soil Properties I-Inside I-Outside II- Inside II- Outside III- Inside III- Outside
0-5 cm
% 0.05cb ± 0.02 0.14b ± 0.00 0.30a ± 0.09 0.22ab ± 0.04 0.14b ± 0.03 0.30a ± 0.02 N
kg/ha 217b ± 60 664a ± 32 715a ± 236 508ab ± 46 554a ± 105 618a ± 116
% 0.40cd ± 0.11 2.37c ± 0.14 7.93a ± 0.31 4.72b ± 1.63 4.08bc ± 0.79 8.61a ± 0.57 C
kg/ha 1693b ± 327 11205a ± 836 18821a ± 2785 11130a ± 3629 16290a ± 3142 17819a ± 4434
C:N ratio 8b ± 1 17ab ± 1 28a ± 10 22ab ± 8 30a ± 8 29a ± 3
pH (H2O) 6.7a ± 0.3 5.4b ± 0.2 5.8b ± 0.7 5.1b ± 0.1 5.7b ± 0.1 5.1b ± 0.2
WHC % 41bc ± 8 50b ± 5 80a ± 3 64ab ± 7 48b ± 1 75a ± 14
5-15 cm
% 0.03cb ± 0.00 0.14abc ± 0.00 0.25a ± 0.06 0.17ab ± 0.05 0.10b ± 0.01 0.18ab ± 0.07 N
kg/ha 231b ± 36 1250a ± 265 1499a ± 151 1351a ± 523 1032a ± 83 1425a ± 364
% 0.87c ± 0.12 2.45bc ± 0.35 8.24a ± 1.51 3.40bc ± 1.78 4.57b ± 0.79 5.54ab ± 0.46 C
kg/ha 6783bc ± 824 22961bc ± 4134 50165a ± 4383 25708b± 10582 46049a ± 10848 44237ab ± 5520
C:N ratio 30ab ± 5 19b ± 7 34ab ± 6 20b ± 9 45a ± 11 33ab ± 10
pH (H2O) 6.8a ± 0.5 5.2b ± 0.1 5.7ab ± 0.9 4.9b ± 0.1 5.6ab ± 0.1 4.7b ± 0.4
WHC % 41b ± 6 51b ± 4 73a ± 7 64a ± 1 46b ± 1 67a ± 2
WHC= water-holding capacity
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even greater for ski run III. The C/N ratios in the 0-5 cm soil layers, which are the most biologically active part, were lowest in inside and outside of ski run III. This is in agreement with C and N content of soil. Andre and Aanderson (1961) reported that granite substratum were the most erosive of eight geological types, as indicated by the ratio of sand surface area and aggregated clay fractions. Moreover, Claassen and Zasoski (1998) pointed out that soil organic matter is a critical factor in aggregation and explained most of differences in levels between barren and revegetated decomposed
granite substratum. Fluctuation of the N mineralization (NH4+-N
and NO3--N) during the 63 days of incubation (0, 21 and 63 days) is shown in Figure 1. The measured NH4+-N amount generally increased in the site outside of the ski runs from beginning toward the end, whereas it was decreased in the inside of the ski runs (Figure 1). Similar results were observed in the 5-15 cm layer of soil as well (Figure 1). The measured NO3--N values of both 0-5 and 5-15 cm soil layers showed an increasing pattern toward 63rd day in both the inside and outside of the ski
Figure 1 The fluctuation of the N mineralization in two soil layers of the inside and outside of the ski runsduring 63 days of incubation (n=3).
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runs (Figure 1). The increase of the NH4+-N on the outsides of the ski runs could be explained by its dominancy in coniferous forest soils. The release of ammonium from decomposing organic material provides the major source of biologically available nitrogen in forest soils (Vitousek and Matson 1985). Additionally, the change in soil NO3--N amount is more significant in the inside of ski run II where the natural revegetation takes place and in the inside of the ski run III where the disturbance was least.
According to net NH4+-N yield values from 21st day to 63rd day among all of the three soil layers of the inside of the ski runs, there is a general
decrease, whereas there is a general increase among the outside ski runs except I-outside (Figure 2). According to net NO3--N yield values from 21st day to 63rd day among all of the three soil layers of the both inside and outside of the ski runs, there is a general increase (Figure 2), but this increase is clearer on ski run II where natural regeneration has taken place and in the inside of the ski run III where disturbance was less.
The tree species inside the forest ecosystem affect N mineralization rates by producing biomass, by accumulating soil organic matter, and by altering its chemical properties (Scott and Binkley 1997, Lovett et al. 2004). The changed N status of a
Figure 2 Comparison of the sample sites regarding their net NH4+-N and NO3--N yield for 21, 42,and 63 day incubation periods (α; 0.05, n=3). [Differences among sample sites are shown by theletters on each bar. Different letters represent the difference groups among sample sites (P<0.05)].
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site may be manifested in litter quality, which reflects species composition and influences rates of decomposition and subsequently rates of N cycling (Aber et al. 1989, Tietema et al. 1992). Hassink (1994) reported that the changes in litter quality resulted in changes in soil organic matter composition, which was associated with N mineralization. The significant NO3--N yield increased in the outsides of ski run I and II, but it was decreased in the outside of the ski run III. This increase was as a result of 100 % forest cover. The plant cover of the undisturbed outsides followed the order: I > II > III, and these differences are expected to be related to levels of litter accumulation. The lowest total net mineral N (NH4++ NO3--N) yield was determined inside ski
run I among all three levels determined in the 0-5 cm soil layer (Figure 3). This suggests an adverse effect of disturbance on mineralization. Moreover, the erosion process causes continuing loss of soil organic matter. The lowest N mineralization rates were found in the inside ski run I inside, in accordance with soil organic C and total N values.
We found that the correlation between soil conditions and net N mineralization have some variations for ammonium and nitrate (Table 2). A positive significant correlation was found between net NH4+-N and total N (r2=0.246), and organic C (r2=0.256) (P<0.05). However, a negative significant correlation was found between pH and NH4+-N (r2=0.318), but it was not significant for WHC (r2=0.209) and C/N ratio (r2=0.063)
Figure 3 Comparison of the sample sites regarding to the net mineral N (NH4++ NO3--N) yield for 21, 42, and 63 day incubation periods (α; 0.05, n=3). [Differences among sample sites are shown by the letters on each bar. Different letters represent the difference groups among sample sites (P<0.05)].
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Table 2 Simple correlation coefficients between NH4+, NO3-, and NH4++NO3--N production (mg Nmin /100 g dry soil / 63 days) and soil properties in the 0-5 cm layer of the soil (n=18, P < 0.05 significant correlation)
Parameters r r2 P Y=a+bx
NH4+-N
Total N 0.496 0.246
(P>0.05). The correlation between net NO3--N and soil properties was only significant for total N (r2=0.655) (P<0.005), but it was not significant for other parameters (P>0.05). Significant positive correlations were found between the net N
mineralization rate and soil parameters [total N (r2=0.655), organic C (r2=0.559), C/N ratio (r2=0.219), and WHC (r2=0.604)] while it was negative only for soil pH (r2=0.489) (P<0.05). Rasmussen et al. (1998) reported that the N mineralization rates are increased with N contents in soil organic matter. Our results showed that the potential nitrification rates were positively affected by N contents in soil organic matter, especially.
Mount Uludağ is one of the rare places because of its plant diversity, and it is also one of the Important Plant Areas (IPAs) of Turkey (Uludağ, IPA 18) (Güleryüz et al. 2005). As a consequence, the alteration of vegetation and soils on ski runs brought about important changes on chemical and physical properties of soil, and N mineralization rates were also negatively affected. Especially, the lowest potential N mineralization
rates, organic C, total N content, and WHC were found in the most damaged ski runs. The high nitrification rates in some ski runs, where the self revegetation has been started by natural processes, were connected to some positive changes in soil properties. The Abies bornmuelleriana forest community is the oldest climax community on Mount Uludağ and very sensitive to destruction. Moreover, WIPF et al. (2005) suggested that the ski run should not be built on the sites with high conservation value.
Acknowledgements
This study was the part of a Research Project (TUR-01-12) carried out by the Uludağ University Department of Biology, Bursa Local Agenda 21 and The Bursa Representative of Chamber of Forest Engineers. It was supported by the United Nations Development, Global Environment Facility, Small Grants Programme.
0.036 NxTot.197.557698.4 N-NH 4 +−=+
Organic C 0.506 0.256 0.032 xOrgC933.1772.2 N-NH 4 +−=+
C/N ratio 0.252 0.063 0.314 NxC /304.0506.0 N-NH 4 +−=+
pH (H2O) -0.564 0.318 0.015 xpH307.1031.64N-NH 4 −=+
WHC (%) 0.457 0.209 0.057 (%)334.0661.13 N-NH 4 xWHC+−=+
NO3--N
Total N 0.431 0.186 0.074 NxTot.664.37322.3 N-NO3 +=−
Organic C 0.335 0.112 0.174 xOrgC968.0017.6 N-NO3 +=−
C/N ratio 0.297 0.088 0.231 NxC /271.0484.4 N-NO3 +=−
pH (H2O) -0.194 0.038 0.439 xpH691.270.25N-NO3 −=−
WHC (%) 0.440 0.193 0.068 (%)243.0001.4 N-NO3 xWHC+−=−
NH4++NO3--N
Total N 0.809 0.655 0.000 NxTot.862.94375.1 N Topl min +−=
Organic C 0.748 0.559 0.000 xOrgC901.2245.3 N Topl min +=
C/N ratio 0.469 0.219 0.049 NxC /575.0978.3 N Topl min +=
pH (H2O) -0.670 0.489 0.001 xpH998.1201.90N Topl min −=
WHC (%) 0.777 0.604 0.000 (%)577.066.17 N Topl min xWHC+−=
WHC= water-holding capacity
60
J. Mt. Sci. (2011) 8: 53–61 DOI: 10.1007/s11629-011-1127-6
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ERRATUM
Erratum to: New findings concerning the Pleistocene
Glaciation of the Leh Basin, Ladakh (34°03' N/77°38' E)
Hermann Achenbach
Geographical Institute, University of Goettingen, Department of High Mountain Geomorphology and Geography, Goldschmidtstr. 5, 37077 Goettingen, Germany
E-mail: [email protected]
© Science Press and Institute of Mountain Hazards and Environment, CAS and Springer-Verlag Berlin Heidelberg 2011 Erratum to: J. Mt. Sci.
DOI: 10.1007/s11629-010-2027-x
In the article, an author’s name is missed from the reference ‘Kuhle, M. 2010. Review on dating methods: Numerical dating in the quaternary geology of High Asia. Journal of Mountain Science 7:105-122.’ The correct reference is ‘Kuhle, M. and Kuhle, S. 2010. Review on dating methods: Numerical dating in the quaternary geology of High Asia. Journal of Mountain Science 7:105-122.’ The online version of the original article can be found at http://dx.doi.org/10.1007/s11629-010-2027-x
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