QUAESTIONES GEOGRAPHICAE 30(3) • 2011

Cold in warming times – state and future challenges in High Arctic coastal geomorphological studies

Ma t e u s z Cz e s ł a w St r z e l e c k i

Adam Mickiewicz University in Poznań, Faculty of Geographical and Geological Sciences, Poland & Durham University, Department of Geography, Quaternary Environmental Change Group, UK

Manuscript received: June 24, 2011 Revised version: September 3, 2011

St r z e l e c k i M.C., Cold shores in warming times – current state and future challenges in High Arctic coastal - morphological studie. Quaestiones Geographicae 30(3), Bogucki Wydawnictwo Naukowe, Poznań, pp. 101–113, 6 Figs. ISBN 978-83-62662-75-3. ISSN 0137-477X. DOI 10.2478/v10117-011-0030-0

Ab s t r a c t . Many of the existing intellectual paradigms regarding the functioning of the polar coastal zone are now out-dated, based on descriptive geomorphology and a limited process-based understanding. Currently, among many components of Arctic landscape adjusting to global warming, the coastal zone is probably the most critical one both in terms of rapidity of environmental change as well as importance for human communities living in circumpolar regions. This issue was often raised during the 4th International Polar Year 2007-2008 and encouraged the scientific community to focus on the state of cold region in more detail. In this paper I summarize the most recent developments in Arctic coastal geomorphology with a particular focus on the Sval- bard and draw attention to the research challenges awaiting further investigation. This paper high- lights the need for a greater understanding of the controls on High Arctic coastal geoecosystems, especially given the potential for accelerated warming and sea-level rise in the coming decades and centuries. Many of presented views benefited from discussions with Professor Andrzej Kostrzewski – to whom this volume is dedicated.

Ke y w o r d s : cold region coastal geomorphology, global warming, sea-level change, High Arctic landscape dyna- mics, Svalbard. Matt Strzelecki, Durham University, Department of Geography, Science Site, South Road, Durham DH1 3LE, UK e-mail: [email protected]

The coasts of neglection curate prediction of future scenarios of global climate change. The tremendous research efforts Understanding the transition of Arctic re- undertaken during the 4th International Polar gions, which in recent years have undergone Year 2007–2008 have revealed that the Arctic is a rapid environmental change in response to cli- already experiencing the strongest air and sea mate warming (Serreze et al. 2000; ACIA 2005; temperature rise on Earth. This process directly NorACIA 2011) is of crucial importance for the and indirectly changes the nature of the Arctic interpretation of Earth system reaction to former coastal zone. Of particular interest is the reac- glaciations and climate shifts as well as more ac- tion of Arctic coastal geoecosystems to increased 102 Ma t e u s z Cz e s ł a w St r z e l e c k i

is a lack of even basic agreement on the efficiency of coastal processes in the high latitudes’ then almost twenty years later Byrne & Dionne (2002) review- ing the state of high latitude coastal geomorphol- ogy still had to admit that coastlines, accounting for at least 30% of the world coasts, have been ne- glected and studies on their nature are very lim- ited. Most recently Lantuit et al. (2011) indicated that only 1% of Arctic coastlines have been inves- tigated in sufficient detail to allow quantitative description of processes operating on them. One of the key messages found in all major papers re- viewing the developments in cold region coastal studies is the need for long-term coastal change monitoring and selection of core geo-indicators which could be analyzed in a unified way - un der the umbrella of a circumpolar observation Fig.1. Simplified map of cold region coasts in the northern network (e.g. John & Sugden 1975, Forbes & hemisphere (modified after Byrne & Dionne 2002). 1 – Extent of winter sea ice cover; 2 – Zone of still relatively poorly Taylor 1994, Trenhaile 1997, Byrne & Dionne studied cold region coasts where the mechanisms controlling coastal 2002, Urdea 2007, Forbes et al. 2011). Though evolution remain unknown; 3 – Zone of relatively well-studied cold knowledge of the response of the coastal zone region coasts with running monitoring programmes, and number of high quality papers published in a last decade. to climate change is fundamental to under- standing polar landscape adjustment to global sediment and nutrient supply from land as well warming, we still cannot precisely measure the as increasing open-water conditions leading to rate and scale of changes for vast areas of the Arc- intensified shoreline erosion and sediment trans- tic. At the heart of the problem lies a mismatch port. The recently published report ‘The State of between out-dated concepts based on short field Arctic 2010 Report’ (Forbes et al. 2011) sug- observations and the lack of the studies linking gests that circumpolar coastal zone (Fig.1) is the Arctic coastal evolution with transformation of key interface in the entire Arctic characterized by Arctic landscape occurring during climate shifts ‘most rapid and severe environmental changes on millennial (glacials/interglacial), decadal (e.g. which have serious implications for communi- changes in atmospheric circulation patterns such ties living on coastal resources’. However, many as NAO/AO) and seasonal (i.e. the duration of of the existing opinions regarding the function- snow cover, high/low precipitation, high/ low ing of polar coasts based on limited observations air temperatures, strong/weak winds etc.) times- are invalid and reduces our ability to understand cales. current mechanisms controlling the present state of this fragile zone and do not deliver any sort of prediction of its future evolution. Not only is ‘Known knowns, known unknowns the number of academic papers on high latitude and unknown unknowns’ coastal environments lower than from temperate and tropical regions, but also their qualitative na- Cold region coasts are typically defined as ture seems to be insufficient to allow numerical ‘those areas where frost and ice processes are active modelling and more sophisticated data analyses. during a period of the year which is sufficient to have In contrast to lower latitude coasts little is known a significant, if not permanent, impact on the near regarding the potential impact of climate and terrestrial, coastal and marine environments’ (Byrne sea-level change on high latitude coastal mar- & Dionne 2002). Several authors (e.g. Forbes & gins. This relative lack of research advance has Taylor 1994, Trenhaile 1997) noticed that many persisted for several decades. This is highlighted morphological aspects (cliffs, , barri- by the remark from Trenhaile (1983) that ‘there ers, , spits, embayments, ) and Co l d s h o r e s i n w a r m i n g t i m e s – c u r r e n t s t a t e a n d f u t u r e c h a l l e n g e s i n Hi g h Ar c t i c c o a s t a l g e o m o r p h o l o g i c a l s t u d i e s 103

Fig. 2. High Arctic coastal environments in northern Billefjorden: 1 – sandstone boulder-strewn in northern Adolfbukta; 2 – plunging metamorphic rock cliffs in northern Adolfbukta; 3 – weathered rock cliffs and mixed -gravel barrier in eastern Petuniabukta; 4 – gravel barrier in eastern Petuniabukta; 5 – tidal flat (right), gravel (middle) and (left) in northern Petuniabukta; 6 – spit platform developing at the mouth of Ebbaelva (background), at the front uplifted beach sequences in NE Petuniabukta; 7 – tidal creek in central part of tidal flat ( northern Petuniabukta); 8 – High Arctic in NE Petuniabukta. 104 Ma t e u s z Cz e s ł a w St r z e l e c k i

Fig. 3. Seasonal changes in polar beach profiles (sketches after Hansom and Kirk 1989) as they adjust to open water condi- tions. On the right examples of different stages of from Petuniabukta (images taken by time-lapse camera installed on Wordiekammen massif in years 2009–2010)

­processes (, currents, waves) operating on estuarine, lacustrine and fluvial environments coasts in cold environments (Fig. 2) are similar (e.g. Dionne 1968, 1969, 1988, 1989; Drake & Mc- to those from lower latitudes. What distinguish- Cann 1982; McCann et al. 1981; McCann & Dale es them, however, are the effects of permafrost, 1986; Dale at al. 2002). Also Arctic beach environ- ground ice, frost action, sea ice, snow cover, iso- ments (Fig. 3) have been solicitously described stasy, glacial history and other zonal factors on in many sites (e.g. Rex 1964; Hume & Schalk . It is important to no- 1964a, 1964b, 1967, 1976; Zenkovitch 1967; King tice that the scientific description of cold region & Buckley 1968; McCann & Owens 1969; Green coastal environments is characterized by many 1970; Owens & McCann 1970; McCann & Taylor discrepancies. For instance, tremendous effort 1975; Rosen 1978; Taylor 1978; Reinson & Rosen of Canadian researchers in last 40 years brought 1982; Sempels 1987; Reimnitz et al. 1990; Barnes a major advance in our understanding of process- et al. 1993, Campeau & Héquette 1995) whereas es controlling Arctic tidal flats and development to date there have been relatively few studies of the term glacielto describe ice-influenced land- investigating Arctic rocky coasts (e.g. Jahn 1961; forms, sediments, processes in marine, coastal, Nielsen 1979; Dionne & Brodeur 1988, Fournier Co l d s h o r e s i n w a r m i n g t i m e s – c u r r e n t s t a t e a n d f u t u r e c h a l l e n g e s i n Hi g h Ar c t i c c o a s t a l g e o m o r p h o l o g i c a l s t u d i e s 105

& Allard 1992, Ødegård & Sollid 1993; Ødegård the wave influence on the Arctic coasts will et al. 1995; Lundberg & Lauritzen 2002; Wagens- continue to intensify with implications for ac- teen et al. 2007; Strzelecki 2011). This gap is even celerated erosion; more profound if we take into consideration that –– the changing Arctic sea-ice regime and the tim- up to 35% of Arctic coastlines are rock-domi- ing of ice break-up and freeze-up may result nated (Lantuit et al. 2011). The classic example in further reduction of coastal protection from showing the research stagnation in revealing the waves (in last decade sea-ice extent reached complexity of high latitude rocky coastal zone is record minima in extent and perennial ice has the longstanding controversy regarding the ori- been reduced by almost 50% in extent); gin of strandflats. This has been a regular topic –– the increased sea-surface temperatures, long- for discussion in the geomorphological literature er ice-free periods and intensified thawing of for almost a century (Nansen 1922; Guilcher et subsea, coastal and inland permafrost leads to al. 1986; Holtedahl 1998) and a debate on the ef- rapid erosion and retreat of Arctic coasts as ficiency of periglacial shoreline evolution, with it was documented in recent years in enthusiasts of slow (Zenkovich 1967) and rela- and Siberia. ACD calculations of mean rates tively rapid evolution (Jahn, 1961). of coastal retreat in the last decades are typi- Furthermore, the development in Arctic cally in the 1–2 m/year range, but vary up to coastal geomorphology is marked by signifi- 10–30 m/year along the Beaufort Sea, the East cant regional contrast. The last decade has seen Siberian Sea, and the Laptev Sea. ACD proved major developments in Arctic coastal research that previous reports underestimated the sed- due to research from the Arctic Coastal Dynam- iment and carbon supply from Arctic coasts to ics (ACD) Group (Rachold et al. 2005; Overduin the ocean; et al. 2007; Lantuit & Pollard 2008, Lantuit et al. –– the existence of a strong link between sea-level 2011). Another important step was the reopen- rise in the Arctic coastal zone and warming of ing of Russian works to the wider scientific com- the coastal waters as well as increased water munity, especially in the field of thermoabrasion freshening; and coasts formed in the Yedoma formation (e.g. –– the rise in sea level is expected to enhance Aré 1988; Nikiforov et al. 2005; Leontiev 2006; Aré coastal erosion and affect sediment transport et al. 2008; Lukyanova et al. 2008; Streletskaya et in coastal areas (various IPCC models show al. 2009). The major focus in these initiatives has higher sea-level rise in the Arctic than mean- been the understanding and modelling of ice-rich global rise); permafrost along Alaskan and Siberian coast- –– glacial legacy (glacioisostatic uplift/subsid- lines. The study by Lantuit et al. (2011) indicated ence) is a dominant factor controlling the rela- that in comparison to Beaufort and Laptev Sea tive sea-level change and is characterized by coastlines, the coasts of High Arctic strong regional contrasts e.g. Canadian Arctic such as Svalbard, Franz Josef Land, the Cana- Archipelago with emerging central part and dian Arctic Archipelago (CAA) and Greenland, submerging margins; whose melting ice masses contribute the most to –– climate warming leads to increased Arctic riv- present-day sea level rise, are still poorly recog- er discharge and sediment supply to the coast- nized. Nevertheless, thanks to research projects al zone. However, in some locations increased carried out by ACD (Fig. 4) we can consider the terrestrial sediment delivery is not sufficient beginning of the 21st century as a golden decade of to balance the negative changes caused by Arctic coastal studies. Their main findings and sea-level rise and storm flooding, what leads predictions from the perspective of coastal geo- to submergence and erosion of Arctic deltas, morphology are: e.g. the second largest Arctic delta, the Mac- –– the expected strong link between Arctic coast- kenzie Delta, is retreating dozens of meters al evolution in coming decades and climate per year. warming; Currently, the leaders of ACD are planning the –– the duration, intensity and number of storms organisation of the Arctic Circumpolar Coastal entering the Arctic has already increased and Observatory Network, which should cover more 106 Ma t e u s z Cz e s ł a w St r z e l e c k i

Fig. 4. Functioning of Arctic coastal zone: A – model developed by Arctic Coastal Dynamics Group for ice-rich permafrost coasts characteristic for Siberian and Alaskan coasts (after Lantuit et al. 2011); B – the complexity of High Arctic coastal adjustment to glacier retreat – no model exists (Photo by Piotr Zagórski, 2010, illustrating paraglacial coastal system in Bellsund, Spitsbergen). sites in the High Arctic and diametrically change High Arctic enigma the regional disproportion. It is then important to ask what kind of research challenges await To date coastal research in High Arctic set- the scientific community along the High Arctic tings has been strongly linked to the successful coasts. application of the paraglaciation concept (sensu Co l d s h o r e s i n w a r m i n g t i m e s – c u r r e n t s t a t e a n d f u t u r e c h a l l e n g e s i n Hi g h Ar c t i c c o a s t a l g e o m o r p h o l o g i c a l s t u d i e s 107

Slaymaker, 2011) in cold region geomorphologi- In recent decades paraglacial processes have be- cal studies. During the 1990s French geomorphol- came one of the most effective geomorphologi- ogists dominated research on High Arctic pa- cal processes on Svalbard, reducing the impact of raglacial coastal systems. Their research focused glacial processes to a secondary role in landscape on the response of the coastal zone to changes in transformation (Laffly & Mercier 2002, Rachle- glacial systems. Héquette & Ruz (1990) and Hé- wicz 2010). Also the previous natural shoreline quette (1992) suggested that although High Arc- protection in the form of sea-ice, ice-foot complex tic coasts are thought to be low energy in a cer- and snow cover now disappear earlier and form tain conditions they can transform very rapidly. later in the season allowing warmer and stormier Their study on coastal margins of glaciofluvial sea conditions to access unconsolidated shore- outwash plains in northwest Spitsbergen (Brøg- lines. ger ) documented a whole mosaic of Based on several environmental monitoring abrupt changes in coastal morphology during case studies on Strokdammane Plain (W Spits- the short Arctic summer with coexisting episodes bergen) Åkerman (2008) proposed a geoeco- of erosion and deposition, formation of new and logical model of Svalbard coasts under global cannibalization of old barriers, deposition of warming conditions (Fig. 5). Åkerman predicts micro-deltas, landward and seaward migration that prolonged duration of the open waters will of coastlines depended on rate of glaciofluvial be critical to the future impacts of coastal and activity in the surrounding and ability of storm near-coastal processes and environments in sites waves to overwash barrier crests. such as Svalbard. With frequent storms abrad- Mercier & Laffly (2005) linked the periods of ing unprotected shores additionally destabilized intensified sediment supply, associated with the by thawing permafrost, flooding of coastal low- post-Little Ice Age (LIA) retreat of Pedersenbreen, lands, high and wide barrier systems blocking Austre, Midre and Vestre Lovénbreen with coastal stream outlets, Svalbard coastal geoecosystem progradation. During the last 30 years, the mean will change rather abruptly. annual coastal progradation along studied section On the other hand, Ziaja et al. (2009) already of Kongsfjorden was 3 m. It has also been noted documented a whole cycle of coastal landscape that in coastal sections where glaciofluvial sedi- transition related to the post-LIA deglaciation of ment delivery was reduced shoreline recession Humbergbukta in SE Sorkapp which highlighted was observed. This study demonstrated the high the role of changes in the High Arctic coastal zone sensitivity of Svalbard coasts to mechanisms con- as a simulator of polar life expansion. Retreat of trolling the supply of sediments from deglaciated Hambergbreen and other surrounding glaciers catchments. In this respect their work confirmed not only led to formation of new coastlines which earlier observations from Atlantic Canada, made quickly become transformed by coastal process- by Forbes and Taylor (1987) who recorded on- es, but also exposed new areas for plant succes- shore migration of gravel barriers during periods sion and animal colonization. of sediment shortage and spit extension after an Another example of Svalbard coastal zone increase in sediment input. In more sheltered area adjustment to climate warming and change in of Spitsbergen, centrally located – Petuniabukta, sediment delivery pathways was a study on the characterized by limited fetch and prolonged decadal–scale shoreline dynamics of Calypsos- sea-ice conditions, Strzelecki (2011) reported tranda carried by Zagórski (2011). His investiga- similar rates of coastal adjustment. This research tions, combining remote sensing and field-based suggests that High Arctic coasts fed by paragla- observations indicated the dominance of coastal cially reworked and transported sediments de- erosion over accumulation with maximum coast- serve a new model, which will properly reflect al retreat up to 100 m, regardless of the retreat the interplay between sediment supply, sea-level of surrounding glaciers and increased sediment change and glacial landscape transition. This is supply to the system. In addition, based on important because many sections of the Svalbard a study of post-LIA geosuccession in Recherfjor- coast are clearly still responding to a combina- den region Zagórski et al. (in preparation) devel- tion of ongoing paraglacial and coastal processes. oped a concept of direct and indirect glacial in- 108 Ma t e u s z Cz e s ł a w St r z e l e c k i

He also postulated a role of high waves in- duced by ice-berg roll from calving in over-wash- ing and reshaping High Arctic coastal barriers, leading to the formation of boulder barricades and beaches. It has to be stated that the role of landslide (paraglacial) or ice-berg induced tsuna- mi waves on the Arctic coastal morphology has never been studied in detail. Later on, Nielsen (1994) expanded his concept of glacier/coastal interaction during the study of Arctic delta in Sermilik Fjord. This is a key work documenting the sensitivity of the high latitude coastal zone to post-LIA landscape transition from glacier into paraglacial dominated geoecosystem and the ra- pidity with which such change can occur. During one century the delta system experienced all stag- es of evolution from rapid formation after retreat of Mitdluagkat glacier; progradation in response to intensified sediment supply; development of spits, barriers, tidal and ; finally to a degradation by waves and currents under ris- ing sea-level conditions after reduction of deliv- ery from glacier catchment. More recently Hansen (2004) illustrated the complexity of a High Arctic delta system response (Hall Bredning–Scoresby Sund, East Greenland) to change in topography, sediment supply, rate of deglaciation and shifts in climate on the Holocene timescale. Hansen’s model can be adapted to hundreds of small and sheltered Arctic deglaciated during the Holocene; it also proves that High Arctic coastal Fig. 5. Scenario of geoecological changes of Svalbard coasts environments may serve as a useful tool in recon- under global warming conditions (modified after Åkerman structing environmental change. 2008). fluence on High Arctic coastal evolution which differentiates coasts formed after retreat of - Stories to be rewritten water glaciers from coasts formed due to intensi- fication of sediment delivery from valley-glacier One of the classic examples of the application systems. The direct influence of glacier systems of sedimentological survey of coastal on the coastal zone was previously documented in palaeogeographical reconstruction is a study by by Nielsen (1992) in West Greenland. The retreat Lønne & Nemec (2004) on High Arctic coastal fan of the tide-water glacier Equip Sermia after the delta in Advenfjorden (Spitsbergen). By detailed 1920s advance led to the transformation of a lat- sedimentological analysis of fan depositional eral moraine into a barrier spit and formation of structures they demonstrated the importance of a lagoon system in just 70 years. Nielsen argued fan deltas as a proxy record of deglaciation his- that such a rapid landform transformation has tory and environmental change in a High Arctic serious implications for Holocene landscape in- terrain, especially important in regions character- terpretation, especially in case of landform and ized by low preservation of glacigenic sediments sediment assemblages related to tide-water gla- and landforms. The small fan system developing cier systems. at the foot of Hiorthfjellet was a very precise re- Co l d s h o r e s i n w a r m i n g t i m e s – c u r r e n t s t a t e a n d f u t u r e c h a l l e n g e s i n Hi g h Ar c t i c c o a s t a l g e o m o r p h o l o g i c a l s t u d i e s 109 corder of the interplay between terrestrial and Action instead of conclusions marine processes adjusting to shifts in sediment delivery from retreating glacier as well as fluc- I strongly believe that the described gap in tuations of a sea–level. This study, apart from understanding of High Arctic coastal adjustment documenting in an unprecedented detail the sed- to global warming conditions represents a great imentology of a polar fan system fed by glacier opportunity for the national polar research com- streams, snow melt and degrading permafrost, munity. Longstanding history of Polish investi- also provided the first well-dated onshore proof gations on Svalbard with environmental moni- for a Mid-Holocene transgression in central Spits- toring programmes running for decades as well bergen. Surprisingly, even after this important as a network of research stations spread across research, the significance of cold region coastal Spitsbergen constitute a solid basis for an inter- fan systems still remains unrecognized. disciplinary research project focusing on the Another important story can be added to re- functioning of the coastal zone in the heart of the construction of polar landscapes by studying European Arctic. Due to its location at the bound- the sedimentology of gravel–dominated storm ary between oceanic and atmospheric fronts, ridges preserved in many uplifted marine se- Svalbard is one of the key areas to study the Arc- quences across High Arctic region. In Andrée- tic sensitivity to climate change. The Svalbard land (NW Spitsbergen) Brückner et al. (2002) and region has, therefore, been an area of many scien- Brückner & Schellmann (2003) postulated that tific breakthroughs including: palaeo-climate re- uplifted beach ridges may help us decipher the constructions (e.g. Isaksson et al. 2005); the extent glacio-isostatic and palaeoceanographic changes. of the last glaciation (e.g. Mangerud et al. 1998; They based their hypothesis on the assumption Svendsen et al. 2004); Holocene sea level changes that conditions favourable for formation of beach (e.g. Forman et al. 2004); modern and relict glacial ridges reflects existence of ice-free conditions as- systems (e.g. Boulton 1972; Lønne & Lyså 2005; sociated with retreat of glacier systems and open- Nuth et al. 2010); periglacial permafrost processes water summer season with wave and current and mechanisms (e.g. Humlum et al., 2003); ocean activity. In the case of Woodfjorden and Wijdef- water interaction and mixing (e.g. Ślubowska- jorden, formation of hundreds of Holocene beach Woldengen et al. 2007, Majewski et al. 2009). ridges was possible only due to climate warming Despite the wealth of research which has been which lead to retreat of the glacier, opening of the undertaken in Svalbard, there remains a lack of fjord and entrance of warm waters brought by investigation into coastal processes and environ- the West Spitsbergen Current securing removal ments. Previous coastal studies (Mercier & Laffly of sea ice and open water conditions in summer 2005, Ziaja et al. 2009, Strzelecki 2011, Zagórski months. More recently St-Hilaire-Gravel et al. 2011) document dramatic changes in sediment (2010) studied the topography and sedimentol- flux and coastal response under intervals char- ogy of uplifted beach ridges on Lowther Island acterised by a warming climate, retreating local (CAA) in order to test their ability to record past ice masses, a shortened winter sea-ice season wave intensity and sea-ice conditions. However, and melting permafrost. These terrestrial proc- reflecting only local conditions they suggested esses are interacting with glacio-isostatic land that better-developed beach ridges can be associ- emergence and on-going global sea-level rise. ated with periods of prolonged wave activity (in- The pristine coasts of Svalbard provide a superb creased duration of ice free periods). One future opportunity to quantify how High Arctic coasts direction of research might be to compare the are responding to rapid climate warming. Never- onshore record (beach ridges, coastal fan deltas) theless several crucial research questions are still with the offshore record from ocean cores collect- to be answered including: What processes control ed across the High Arctic to shed new light on the existing Svalbard coasts?; How sensitive is the Sval- history of sea ice and ocean currents. bard coastal zone to recent increased human impact?; 110 Ma t e u s z Cz e s ł a w St r z e l e c k i

What was the response of the Svalbard coastal zone to friendship and helping me aim only for the high- intensified glacial recession and sediment supply after est goals. the Little Ice Age?; Do coastal processes intensify the Gratitiude is directed to Crescendum Est- Po- rate of rock weathering on Svalbard climates?; How lonia Foundation, Adam Mickiewicz University did the Svalbard coast and respond Foundation, Ministry of Science and Higher Edu- to climate change, glacier fluctuations and sea ice cation in Poland (grant no. N306284335), Nation- changes throughout the Holocene?; What is the preci- al Environmental Research Council in UK and sion of the morphological and sedimentological records Ustinov College at Durham University support- of environmental transformations, climate change and ing my research and career development. natural disasters along the Svalbard coast? I also thank Jerry Lloyd who gave critical These research premises and challenges led to comments on an earlier version of the manu- the formation of a SVALCOAST research team script. Review by Wiesław Ziaja also improved linking geoscientists from leading national po- the manuscript and is highly appreciated. lar research institutions and international scien- tific partners which in coming years will aim to examine the response of the coastal zone of the References Svalbard Archipelago to current climatic warm- Åk e r m a n J.H., 2008. Coastal Processes and Their Influence ing and multidirectional anthropopression and Upon Discharge Characteristics of the Strokdammane explore the changes experienced by the , West Spitsbergen, Svalbard. Proceedings of the Ninth landscape during various stages of deglaciation. International Conference on Permafrost University of Alaska Fairbanks June 29–July 3, 2008 1: 19–24. As well as this, predictions will be made as to Arctic Climate Impact Assessment (ACIA) ScientificReport, 2005. the coast’s future evolution under scenarios of Cambridge University Press, Cambridge. continuing increases in air temperature and sea- Ar é F.E., 1988. Thermal abrasion of sea coasts. Polar Geogra- level rise (Strzelecki & Zagórski 2011). Given the phy and Geology 12: 1–157. Ar é F.E., Re i m n i t z E., Gr i g o r i e v M., Hu b b e r t e n H.-W., Ra- diversity of research questions and rapidity of c h o l d V., 2008. The influence of cryogenic processes on coastal adjustment it seems to be a fascinating the erosional Arctic shoreface. Journal of Coastal Research challenge! 24: 110–121. Ba r n e s P.W., Ke m p e n a E.W., Re i m n i t z E., Mc c o r m i c k M., We- b e r W.S. & Ha y d e n E.C., 1993. Beach profile modification and sediment transport by ice: an overlooked process on Acknowledgements Lake Michigan. Journal of Coastal Research 9: 65–86. Bo u l t o n G.S., 1972. Modern Arctic glaciers as depositional models for former ice sheets. Journal of Geological Society I would like to thank Professor Andrzej Kos- London 128: 361–393. trzewski for many years of excellent supervision, Br ü c k n e r H. & Sc h e l l m a n n G., 2003. Late Pleistocene and Holocene shorelines of Andréeland, Spitsbergen (Sval- bard) – eomorphological evidence and palaeo-oceano- graphic significance. Journal of Coastal Research 19: 971– 982. Br ü c k n e r H., Sc h e l l m a n n G. & v a n d e r Bo r g K., 2002. ���Up- lifted beach ridges in northern Spitsbergen as indicators for glacio-isostasy and palaeo-oceanography. Zeitschrift für Geomorphologie 46: 309–336. By r n e M.-L. & Di o n n e J.-C., 2002. Typical Aspects of Cold regions Shorelines. In: K. Hewitt, M.-L. Byrne, M. Eng- lish, G. Young (eds.), Landscapes in Transition. Landform Assembladges and Transformations in Cold Regions. Kluver Academic Publishers, Dordrecht: 141–158. Ca m p e a u S. & Hé q u e t t e A., 1995. Buttes cryogènes saison- nières de plages arctiques, péninsule de Tuktoyaktuk, Territoires du Nord-Ouest. Géographie physique et Quater- naire 49: 265–274. Da l e J.E., Le e c h S., McCa n n B. & Sa m u e l s o n G., 2002. Sedi- mentary characteristics, biological zonation and physi- cal processes of the tidal flats of Iqaluit, Nunavut. In: K. Fig. 6. Prof. Andrzej Kostrzewski and Matt Strzelecki dur- Hewitt, M.-L. Byrne, M. English, G. Young (eds.), Land- ing geomorphological mapping of western coast of Petu- scapes in Transition. Landform Assembladges and Transfor- niabukta, Spitsbergen August 2007. Co l d s h o r e s i n w a r m i n g t i m e s – c u r r e n t s t a t e a n d f u t u r e c h a l l e n g e s i n Hi g h Ar c t i c c o a s t a l g e o m o r p h o l o g i c a l s t u d i e s 111

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