DOCSLIB.ORG

10Be Exposure Age Chronology of the Last Glaciation of the Roháčská Valley in MARK the Western Tatra Mountains, Central Europe

Total Page：16

File Type：pdf, Size：1020Kb

Download full-text PDF Read full-text
10Be Exposure Age Chronology of the Last Glaciation of the Roháčská Valley in MARK the Western Tatra Mountains, Central Europe Geomorphology 293 (2017) 130–142 Contents lists available at ScienceDirect Geomorphology journal homepage: www.elsevier.com/locate/geomorph 10Be exposure age chronology of the last glaciation of the Roháčská Valley in MARK the Western Tatra Mountains, central Europe ⁎ Zbyněk Engela, , Pavel Mentlíkb, Régis Braucherc, Marek Křížeka, Markéta Pluháčkováb, Aster Teamc a Charles University, Faculty of Science, Department of Physical Geography and Geoecology, Albertov 6, 12843 Praha, Czech Republic b University of West Bohemia, Center of Biology, Geoscience and Environmental Education, Klatovská 51, 30619 Plzeň, Czech Republic c Aix Marseille Université, CNRS, IRD, Collége de France, 13545 Aix-en-Provence cedex 4, France ARTICLE INFO ABSTRACT Keywords: 10Be exposure ages from moraines and bedrock sites in the Roháčská Valley provide chronology of the last Quaternary glaciation in the largest valley of the Western Tatra Mts., the Western Carpathians. The minimum apparent Cosmogenic nuclides exposure age of 19.4 ± 2.1 ka obtained for the oldest sampled boulder and the mean age of 18.0 ± 0.8 ka Glaciation chronology calculated for the terminal moraine indicate that the oldest preserved moraine was probably deposited at the Western Tatra Mts. time of the global Last Glacial Maximum (LGM). The age of this moraine coincides with the termination of the Carpathians maximum glacier expansion in other central European ranges, including the adjacent High Tatra Mts. and the Alps. The equilibrium line altitude (ELA) of the LGM glacier in the Roháčská Valley, estimated at 1400–1410 m a.s.l., was 50–80 m lower than in the eastern part of the range, indicating a positive ELA gradient from west to east among the north-facing glaciers in the Tatra Mts. Lateglacial glacier expansion occurred no later than 13.4 ± 0.5 ka and 11.9 ± 0.5 ka, as indicated by the mean exposure ages calculated for re-advance moraines. This timing is consistent with the exposure age chronology of the last Lateglacial re-advance in the High Tatra Mts., Alps and lower mountain ranges in central Europe. The ELA in the Roháčská Valley estimated at 1690–1770 m a.s.l. in this period was located 130–300 m lower than in the north-facing valleys in the High Tatra Mts. 10Be exposure ages obtained for a rock glacier constrains the timing of this landform stabilization in the Salatínska Valley and provides the first chronological evidence for the Lateglacial activity of rock glaciers in the Carpathians. 1. Introduction confidently dated. Despite the wide application of cosmogenic nuclide dating in the Reconstructions of the past glacier variability are among the most field of glacial geology over the past three decades (Ivy-Ochs et al., useful records of paleoclimate changes during the Quaternary. In 2014), the chronology of glaciations remains poorly constrained in mountain regions, glacier history is often the primary proxy for climate many mountain regions. A large data set of exposure ages on glacial during glacial periods. Mountain glaciers are a particularly important deposits exists from the Andes (e.g. Rodbell et al., 2009 and references paleoclimate proxy for two reasons. First, glaciers are the key climate therein; Fernández and Mark, 2016), the Cordilleras in the western U.S. indicators, retreating and advancing in response to changes in the (Balco, 2011; Rood et al., 2011; Young et al., 2011), High Asia glacier mass balance, which is mainly determined by snow accumula- (Chevallier et al., 2011; Heyman, 2014; Owen and Dortch, 2014) and tion (precipitation) and glacier melt (air temperature) over a year (e.g. Scandinavia (Hughes et al., 2016; Stroeven et al., 2016), but other Winkler et al., 2010). Second, geomorphic evidence of glacier advances ranges are yet underexplored. Limited chronological data are available such as ice marginal landforms, polished bedrock surfaces and trimlines for the Carpathians, the largest mountain region in mainland Europe. is the only well-preserved palaeoclimate proxy for glacial periods in The glaciation history of this range has been an object of glacial studies many mountain systems, which generally retain poor sedimentary since the mid-19th century when Zejszner (1856) recognized the records. Glacier history is considered a reliable indicator of climate existence of former glaciers in the Tatra Mts. (Fig. 1, inset), the Western changes in those ranges, where glacier deposits are widespread and Carpathians. There were a number of geomorphological investigations ⁎ Corresponding author. E-mail address: [email protected] (Z. Engel). Maurice Arnold, nk> http://dx.doi.org/10.1016/j.geomorph.2017.05.012 Received 10 November 2016; Received in revised form 15 May 2017; Accepted 19 May 2017 Available online 24 May 2017 0169-555X/ © 2017 Elsevier B.V. All rights reserved. Z. Engel et al. Geomorphology 293 (2017) 130–142 Fig. 1. Overview of the Western Tatra Mts. range and its position in the Carpathians of central Europe (grey shade, inset map). The LGM extent of glaciers in the Tatra Mts. and central Europe (blue shades, inset map) is after Zasadni and Kłapyta (2014) and Ehlers et al. (2011), respectively. The valleys cited in the paper are indicated by full names or abbreviations (DK: Kondratowa, DSK: Sucha Kasprowa, DG: Gąsienicowa, DPSP: Pięciu Stawów Polskich Valley, DM: Za Mnichem). A red box indicates the outline of Figs. 2 and 6 and a dashed line marks the water divide. (For interpretation of the references to colour in this figure legend, the reader is referred to the web version of this article.) of the glacial landscape within the Carpathians during the next decades glaciers and a bedrock surface in the Roháčská Valley, the largest area (e.g. Sawicki, 1911; Lukniš, 1964; Sîrcu, 1964), but no chronological of Quaternary glaciation in the Western Tatra Mts. We thus establish a evidence was reported from this region until the beginning of the 21st new glaciation chronology for the valley spanning the LGM and century (Reuther et al., 2007; Urdea and Reuther, 2009; Rinterknecht Lateglacial. We compare the derived chronology with published et al., 2012; Kuhlemann et al., 2013; Gheorghiu et al., 2015; chronological data on local glaciations in both the Western and High Ruszkiczay-Rüdiger et al., 2016). Tatra Mts. and we interpret our findings with respect to the results of The Tatra Mts. have been the most extensively glaciated part of the the recent paleoclimate studies from the Carpathians and Alps. Carpathians during the Quaternary. The large extent of local glaciations resulted from high topography of the range (the maximum elevation of 2. Study area 2655 m a.s.l.) and their location in the north-western part of the Carpathians exposed to humid air masses moving in from the Atlantic The Western Tatra Mts. (49°08′–49°17′ N, 19°34′–20°00′ E) are a Ocean. A number of cirque and valley glaciers formed along the divide 30 km-long and 16 km-wide range in the northernmost part of the (Zasadni and Kłapyta, 2014) leaving a strong erosional imprint on the Carpathians. The range extends between 790 and 2248 m a.s.l. (Bystrá landscape. The strong geomorphological evidence left by former ice Mountain; Fig. 1). The range extends from the western part of the High masses makes the Tatra Mts. a primary focus of palaeoglaciological Tatra Mts., the highest part of the Carpathians. The southern part of the research in the Carpathians. In this region, the first reconstructions of range is built of Proterozoic gneisses, schist and amphibolite while the the spatial extent of local glaciers were achieved (Partsch, 1882; Dénes, main ridge consists of polygenetic Variscan granitoids (Jurewicz, 1902) and different palaeoglacial histories have been suggested (Dénes, 2007). The crystalline basement is overlain by Mesozoic sedimentary 1902; de Martonne, 1911; Partsch, 1923; Romer, 1929). sequences which consist of an autochthonous sedimentary cover, the The number and likely age of Quaternary glaciations in the Tatra High-Tatric and Krížna nappes in the western and northern part of the Mts. were initially assessed based on geomorphologic criteria (Halicki, range (Putiš, 1992). In the topographic sense the Tatra Mts. emerged 1930; Lukniš, 1959; Klimaszewski, 1960) or weathering characteristics due to a Miocene rotational uplift that resulted in an asymmetric horst of moraine material (Lukniš, 1973). Krupiński (1984) and Baumgart- structure of the massif (Králiková et al., 2014). The massif is deeply Kotarba and Kotarba (1993, 1995, 1997) published the first radio- incised by glacial valleys and cirques with headwalls up to 600 m high carbon data from moraine-dammed lakes, providing minimum age (Křížek and Mida, 2013), displaying the most pronounced glacial constraints on the termination of the last glaciation. Further progress morphology within the Carpathians. However, glacierization at present was made when glacier advances were constrained in selected valleys only consists of glacierets or firn-ice patches below north-facing rock using thermoluminescence (Prószyńska-Bordas et al., 1988; Butrym walls (Gądek, 2008). et al., 1990; Lindner et al., 1990, 1993; Lindner, 1994) and optically The climate in the Western Tatra Mts. is transitional between stimulated luminescence techniques (Baumgart-Kotarba and Kotarba, maritime and continental influences. The range represents an oro- 2001). Exposure-age dating applied to glacial landforms since the end graphic barrier to air masses moving in from the Atlantic Ocean, which of 1990s allowed for reconstruction of the glaciation history in selected results in higher precipitation on the northern flank compared to the sites within the range (Dzierżek et al., 1999; Baumgart-Kotarba and southern slopes (Konček et al., 1974). Mean annual precipitation Kotarba, 2001; Dzierżek, 2009; Makos et al., 2013a, 2013b, 2014; Engel generally increases with altitude from 900 to 960 mm at the southern et al., 2015). Makos et al. (2016) published the first exposure ages from foothills (Vido et al., 2015) up to ~1800 mm at Kasprowy Wierch the Kondratowa, Sucha Kasprowa and Bystra Woda valleys in the summit (1991 m a.s.l.; Żmudzka, 2011).
Load more

Recommended publications
  • The Last Maximum Ice Extent and Subsequent Deglaciation of the Pyrenees: an Overview of Recent Research
    Cuadernos de Investigación Geográfica 2015 Nº 41 (2) pp. 359-387 ISSN 0211-6820 DOI: 10.18172/cig.2708 © Universidad de La Rioja THE LAST MAXIMUM ICE EXTENT AND SUBSEQUENT DEGLACIATION OF THE PYRENEES: AN OVERVIEW OF RECENT RESEARCH M. DELMAS Université de Perpignan-Via Domitia, UMR 7194 CNRS, Histoire Naturelle de l’Homme Préhistorique, 52 avenue Paul Alduy 66860 Perpignan, France. ABSTRACT. This paper reviews data currently available on the glacial fluctuations that occurred in the Pyrenees between the Würmian Maximum Ice Extent (MIE) and the beginning of the Holocene. It puts the studies published since the end of the 19th century in a historical perspective and focuses on how the methods of investigation used by successive generations of authors led them to paleogeographic and chronologic conclusions that for a time were antagonistic and later became complementary. The inventory and mapping of the ice-marginal deposits has allowed several glacial stades to be identified, and the successive ice boundaries to be outlined. Meanwhile, the weathering grade of moraines and glaciofluvial deposits has allowed Würmian glacial deposits to be distinguished from pre-Würmian ones, and has thus allowed the Würmian Maximum Ice Extent (MIE) –i.e. the starting point of the last deglaciation– to be clearly located. During the 1980s, 14C dating of glaciolacustrine sequences began to indirectly document the timing of the glacial stades responsible for the adjacent frontal or lateral moraines. Over the last decade, in situ-produced cosmogenic nuclides (10Be and 36Cl) have been documenting the deglaciation process more directly because the data are obtained from glacial landforms or deposits such as boulders embedded in frontal or lateral moraines, or ice- polished rock surfaces.
    [Show full text]
  • Introduction to Geological Process in Illinois Glacial
    INTRODUCTION TO GEOLOGICAL PROCESS IN ILLINOIS GLACIAL PROCESSES AND LANDSCAPES GLACIERS A glacier is a flowing mass of ice. This simple definition covers many possibilities. Glaciers are large, but they can range in size from continent covering (like that occupying Antarctica) to barely covering the head of a mountain valley (like those found in the Grand Tetons and Glacier National Park). No glaciers are found in Illinois; however, they had a profound effect shaping our landscape. More on glaciers: http://www.physicalgeography.net/fundamentals/10ad.html Formation and Movement of Glacial Ice When placed under the appropriate conditions of pressure and temperature, ice will flow. In a glacier, this occurs when the ice is at least 20-50 meters (60 to 150 feet) thick. The buildup results from the accumulation of snow over the course of many years and requires that at least some of each winter’s snowfall does not melt over the following summer. The portion of the glacier where there is a net accumulation of ice and snow from year to year is called the zone of accumulation. The normal rate of glacial movement is a few feet per day, although some glaciers can surge at tens of feet per day. The ice moves by flowing and basal slip. Flow occurs through “plastic deformation” in which the solid ice deforms without melting or breaking. Plastic deformation is much like the slow flow of Silly Putty and can only occur when the ice is under pressure from above. The accumulation of meltwater underneath the glacier can act as a lubricant which allows the ice to slide on its base.
    [Show full text]
  • Sea Level and Global Ice Volumes from the Last Glacial Maximum to the Holocene
    Sea level and global ice volumes from the Last Glacial Maximum to the Holocene Kurt Lambecka,b,1, Hélène Roubya,b, Anthony Purcella, Yiying Sunc, and Malcolm Sambridgea aResearch School of Earth Sciences, The Australian National University, Canberra, ACT 0200, Australia; bLaboratoire de Géologie de l’École Normale Supérieure, UMR 8538 du CNRS, 75231 Paris, France; and cDepartment of Earth Sciences, University of Hong Kong, Hong Kong, China This contribution is part of the special series of Inaugural Articles by members of the National Academy of Sciences elected in 2009. Contributed by Kurt Lambeck, September 12, 2014 (sent for review July 1, 2014; reviewed by Edouard Bard, Jerry X. Mitrovica, and Peter U. Clark) The major cause of sea-level change during ice ages is the exchange for the Holocene for which the direct measures of past sea level are of water between ice and ocean and the planet’s dynamic response relatively abundant, for example, exhibit differences both in phase to the changing surface load. Inversion of ∼1,000 observations for and in noise characteristics between the two data [compare, for the past 35,000 y from localities far from former ice margins has example, the Holocene parts of oxygen isotope records from the provided new constraints on the fluctuation of ice volume in this Pacific (9) and from two Red Sea cores (10)]. interval. Key results are: (i) a rapid final fall in global sea level of Past sea level is measured with respect to its present position ∼40 m in <2,000 y at the onset of the glacial maximum ∼30,000 y and contains information on both land movement and changes in before present (30 ka BP); (ii) a slow fall to −134 m from 29 to 21 ka ocean volume.
    [Show full text]
  • A New Greenland Ice Core Chronology for the Last Glacial Termination ———————————————————————— S
    JOURNAL OF GEOPHYSICAL RESEARCH, VOL. ???, XXXX, DOI:10.1029/2005JD006079, A new Greenland ice core chronology for the last glacial termination ———————————————————————— S. O. Rasmussen1, K. K. Andersen1, A. M. Svensson1, J. P. Steffensen1, B. M. Vinther1, H. B. Clausen1, M.-L. Siggaard-Andersen1,2, S. J. Johnsen1, L. B. Larsen1, D. Dahl-Jensen1, M. Bigler1,3, R. R¨othlisberger3,4, H. Fischer2, K. Goto-Azuma5, M. E. Hansson6, and U. Ruth2 Abstract. We present a new common stratigraphic time scale for the NGRIP and GRIP ice cores. The time scale covers the period 7.9–14.8 ka before present, and includes the Bølling, Allerød, Younger Dryas, and Early Holocene periods. We use a combination of new and previously published data, the most prominent being new high resolution Con- tinuous Flow Analysis (CFA) impurity records from the NGRIP ice core. Several inves- tigators have identified and counted annual layers using a multi-parameter approach, and the maximum counting error is estimated to be up to 2% in the Holocene part and about 3% for the older parts. These counting error estimates reflect the number of annual lay- ers that were hard to interpret, but not a possible bias in the set of rules used for an- nual layer identification. As the GRIP and NGRIP ice cores are not optimal for annual layer counting in the middle and late Holocene, the time scale is tied to a prominent vol- canic event inside the 8.2 ka cold event, recently dated in the DYE-3 ice core to 8236 years before A.D.
    [Show full text]
  • Late Quaternary Changes in Climate
    SE9900016 Tecnmcai neport TR-98-13 Late Quaternary changes in climate Karin Holmgren and Wibjorn Karien Department of Physical Geography Stockholm University December 1998 Svensk Kambranslehantering AB Swedish Nuclear Fuel and Waste Management Co Box 5864 SE-102 40 Stockholm Sweden Tel 08-459 84 00 +46 8 459 84 00 Fax 08-661 57 19 +46 8 661 57 19 30- 07 Late Quaternary changes in climate Karin Holmgren and Wibjorn Karlen Department of Physical Geography, Stockholm University December 1998 Keywords: Pleistocene, Holocene, climate change, glaciation, inter-glacial, rapid fluctuations, synchrony, forcing factor, feed-back. This report concerns a study which was conducted for SKB. The conclusions and viewpoints presented in the report are those of the author(s) and do not necessarily coincide with those of the client. Information on SKB technical reports fromi 977-1978 {TR 121), 1979 (TR 79-28), 1980 (TR 80-26), 1981 (TR81-17), 1982 (TR 82-28), 1983 (TR 83-77), 1984 (TR 85-01), 1985 (TR 85-20), 1986 (TR 86-31), 1987 (TR 87-33), 1988 (TR 88-32), 1989 (TR 89-40), 1990 (TR 90-46), 1991 (TR 91-64), 1992 (TR 92-46), 1993 (TR 93-34), 1994 (TR 94-33), 1995 (TR 95-37) and 1996 (TR 96-25) is available through SKB. Abstract This review concerns the Quaternary climate (last two million years) with an emphasis on the last 200 000 years. The present state of art in this field is described and evaluated. The review builds on a thorough examination of classic and recent literature (up to October 1998) comprising more than 200 scientific papers.
    [Show full text]
  • Behavior of the James Lobe, South Dakota During Termination I
    Behavior of the James Lobe, South Dakota during Termination I A dissertation submitted to the Graduate School of the University of Cincinnati in partial fulfillment of the requirements for the degree of DOCTOR OF PHILOSOPHY in the Department of Geology of the McMicken College of Arts and Sciences by Stephanie L. Heath MSc., University of Maine BSc., University of Maine July 18, 2019 Dissertation Committee: Dr. Thomas V. Lowell Dr. Aaron Diefendorf Dr. Aaron Putnam Dr. Dylan Ward i ABSTRACT The Laurentide Ice Sheet was the largest ice sheet of the last glacial period that terminated in an extensive terrestrial margin. This dissertation aims to assess the possible linkages between the behavior of the southern Laurentide margin and sea surface temperature in the adjacent North Atlantic Ocean. Toward this end, a new chronology for the westernmost lobe of the Southern Laurentide is developed and compared to the existing paradigm of southern Laurentide behavior during the last glacial period. Heath et al., (2018) address the question of whether the terrestrial lobes of the southern Laurentide Ice Sheet margin advanced during periods of decreased sea surface temperature in the North Atlantic. This study establishes the pattern of asynchronous behavior between eastern and western sectors of the southern Laurentide margin and identifies a chronologic gap in the western sector. This is the first comprehensive review of the southern Laurentide margin since Denton and Hughes (1981) and Mickelson and Colgan (2003). The results of Heath et al., (2018) also revealed the lack of chronologic data from the Lobe, South Dakota, the westernmost lobe of the southern Laurentide margin.
    [Show full text]
  • Terminal Moraine North America
    Terminal Moraine North America Apothegmatical and roasted Mohan boning: which Franklin is unrequisite enough? Is Wallace civilized or soaringly.dandyish when slurs some states josh rurally? Saxe heartens her sacrament something, she conceptualised it Glacial episode was notcovered with the north america Moraine Wikipedia. Till exposure in mountainous terrain outline of terminal line can be seen of those shown to the inner moraine, augmented by encroachment of terminal moraine north america. Material is from landscape features would soil development, carrying forward great quantities of terminal moraines formed, leveling and terminal moraine in the beach ridges and sedges, parallel to eventually stabilized by planting dune in? The most recent date from bedrock and their associated with no related to publish your response to see a terminal moraine north america bulletin, way through melting. Terminal Moraine A youth of end moraine where a robust or glacial lobe. Eolian deposition of terminal moraine north america. This moraine at the terminal moraine belt, then ran straight westward along. Since the dunes were laid down or formed in some of the ice sheets or beds encountered by two terminal moraine north america over the laurentide ice? That it pretty much like this ice came here way the terminal moraine north america that you are so narrow and terminal moraines. Moraines lack of terminal moraine, structures of terminal moraine north america was derived from among these landscapes. Recessional moraines arrowed marking the shrinkage of a South sun valley already The runway not shown retreated towards the. They were sculpted by the largest of terminal moraine north america almost in? Midwest might look at first glacier has gained wide range over north america during its terminal moraine north america be? The terminal and terminal moraine north america.
    [Show full text]
  • A Glacier Runs Through It: Effects of Late Wisconsinan Glaciation on Stream Drainage Near the Terminal Moraine Boundary in North Central Pennsylvania
    University of Pennsylvania ScholarlyCommons Master of Environmental Studies Capstone Department of Earth and Environmental Projects Science May 2008 A Glacier Runs Through It: Effects of Late Wisconsinan Glaciation on Stream Drainage Near the Terminal Moraine Boundary in North Central Pennsylvania Krista Heinlen University of Pennsylvania, [email protected] Follow this and additional works at: https://repository.upenn.edu/mes_capstones Heinlen, Krista, "A Glacier Runs Through It: Effects of Late Wisconsinan Glaciation on Stream Drainage Near the Terminal Moraine Boundary in North Central Pennsylvania" (2008). Master of Environmental Studies Capstone Projects. 21. https://repository.upenn.edu/mes_capstones/21 Presented to the Faculties of the University of Pennsylvania in Partial Fulfillment of the Requirements for the Degree of Master of Environmental Studies 2007. This paper is posted at ScholarlyCommons. https://repository.upenn.edu/mes_capstones/21 For more information, please contact [email protected]. A Glacier Runs Through It: Effects of Late Wisconsinan Glaciation on Stream Drainage Near the Terminal Moraine Boundary in North Central Pennsylvania Abstract Stream morphology in north central Pennsylvania has been influenced yb the passage of multiple glaciers during the Quaternary period, and most recently by the Late Wisconsinan ice sheet which began to recede just 10,000 years ago. While glaciers can take a heavy erosive toll on the landscape, the Late Wisconsinan and previous glaciers stopped when they reached Pennsylvania, and as such were not as thick and did not cover the ground as long as in regions to the north. This paper examines current morphology in an area along the north central part of the state that contains both glaciated and non-glaciated regions.
    [Show full text]
  • A Glacial-Process Model: the Role of Spatial and Temporal Variations in Glacier Thermal Regime
    A glacial-process model: The role of spatial and temporal variations in glacier thermal regime H. D. MOOERS Department of Geology and Geophysics, 108 Pillsbury Hall and Limnological Research Center, 220 Pillsbury Hall University of Minnesota, Minneapolis, Minnesota 55455 ABSTRACT ucts of glaciation also provide important infor- there are several distinct thermal environments, mation on the physical nature and dynamics of each of which has a dominant set of erosional or Glacial landform assemblages associated the ice. Moran (1971), Clayton and Moran depositional processes. The position and charac- with the retreat of the Rainy and Superior (1974, 1977), and Moran and others (1980) teristics of these zones also vary with time during lobes of the Laurentide Ice Sheet in Minne- used field relationships to reconstruct the glacio- glacial advance and retreat. sota provide a record of spatial and temporal logical conditions necessary for the formation of The glacial sediments and landforms in Min- variations in glaciological processes. The large-scale glaciotectonic features, and they pro- nesota associated with the late Wisconsin St. two lobes advanced contemporaneously to vided a major advance in the understanding of Croix Phase provide a detailed record of the their maximum at the St. Croix moraine. The ice-marginal glacial processes. Mathews (1974) maximum and recessional events of the Superior portion of the moraine formed by the Rainy reconstructed longitudinal profiles of the Lau- and Rainy lobes. During recession, each major lobe is characterized by large frontal outwash rentide Ice Sheet and changed the way subse- lobe broke up into multiple, smaller sublobes, plains, broad ice-stagnation topography, gla- quent researchers have viewed ice lobes along its dynamically independent from one another.
    [Show full text]
  • Article Is Available Online USA, 2004
    The Cryosphere, 10, 639–664, 2016 www.the-cryosphere.net/10/639/2016/ doi:10.5194/tc-10-639-2016 © Author(s) 2016. CC Attribution 3.0 License. Numerical simulations of the Cordilleran ice sheet through the last glacial cycle Julien Seguinot1,2,3, Irina Rogozhina3,4, Arjen P. Stroeven2, Martin Margold2, and Johan Kleman2 1Laboratory of Hydraulics, Hydrology and Glaciology, ETH Zürich, Zürich, Switzerland 2Department of Physical Geography and the Bolin Centre for Climate Research, Stockholm University, Stockholm, Sweden 3Helmholtz Centre Potsdam, GFZ German Research Centre for Geosciences, Potsdam, Germany 4Center for Marine Environmental Sciences, University of Bremen, Bremen, Germany Correspondence to: Julien Seguinot ([email protected]) Received: 21 June 2015 – Published in The Cryosphere Discuss.: 7 August 2015 Revised: 2 February 2016 – Accepted: 19 February 2016 – Published: 16 March 2016 Abstract. After more than a century of geological research, 1 Introduction the Cordilleran ice sheet of North America remains among the least understood in terms of its former extent, volume, and dynamics. Because of the mountainous topography on During the last glacial cycle, glaciers and ice caps of the which the ice sheet formed, geological studies have often had North American Cordillera have been more extensive than only local or regional relevance and shown such a complexity today. At the Last Glacial Maximum (LGM), a continuous that ice-sheet-wide spatial reconstructions of advance and re- blanket of ice, the Cordilleran ice sheet (Dawson, 1888), treat patterns are lacking. Here we use a numerical ice sheet stretched from the Alaska Range in the north to the North model calibrated against field-based evidence to attempt a Cascades in the south (Fig.1).
    [Show full text]
  • Rapid Laurentide Ice-Sheet Advance Towards Southern Last Glacial Maximum Limit During Marine Isotope Stage 3
    Quaternary Science Reviews 196 (2018) 118e123 Contents lists available at ScienceDirect Quaternary Science Reviews journal homepage: www.elsevier.com/locate/quascirev Rapid Laurentide ice-sheet advance towards southern last glacial maximum limit during marine isotope stage 3 * Anders E. Carlson a, , Lev Tarasov b, Tamara Pico c a College of Earth, Ocean, and Atmospheric Sciences, Oregon State University, USA b Department of Physics and Physical Oceanography, Memorial University, Canada c Department of Earth and Planetary Sciences, Harvard University, USA article info abstract Article history: Marine isotope stage (MIS) 3 (~58e28 ka) is a period of intermediate global ice volume between MIS 4 Received 21 February 2018 and the last glacial maximum of MIS 2. Here we report geologic evidence for southern Laurentide ice- Received in revised form sheet rapid growth to near its last glacial maximum extent after a period with limited ice in the 23 April 2018 southernmost Hudson Bay lowland. A14C age on wood in lacustrine sediments interbedded with glacial Accepted 29 July 2018 tills in central-eastern Wisconsin dates a Laurentide ice-sheet advance southwards to an extent at least Available online 7 August 2018 equivalent to at least its ~17 ka deglacial limit by 39.1 ± 0.4 ka. This advance ended before 30.4 ± 0.9 ka based on another 14C date on wood in lacustrine sediment overlying the till layers. This advance is consistent with 14C ages from Michigan and Iowa, and Gulf of Mexico runoff records that support a concurrent southern Laurentide ice-sheet advance. We infer changes in North American ice volume using ice-sheet model simulations from a large ensemble that are consistent with 14C-data and Gulf of Mexico- discharge constraints.
    [Show full text]
  • Lower Oceanic Δ13 C During the Last Interglacial Period Compared to The
    Clim. Past, 17, 507–528, 2021 https://doi.org/10.5194/cp-17-507-2021 © Author(s) 2021. This work is distributed under the Creative Commons Attribution 4.0 License. Lower oceanic δ13C during the last interglacial period compared to the Holocene Shannon A. Bengtson1,2, Laurie C. Menviel1, Katrin J. Meissner1,2, Lise Missiaen1, Carlye D. Peterson3, Lorraine E. Lisiecki4, and Fortunat Joos5,6 1Climate Change Research Centre, The University of New South Wales, Sydney, Australia 2The Australian Research Council Centre of Excellence for Climate Extremes, Sydney, Australia 3Earth Sciences, University of California, Riverside, California, USA 4Department of Earth Science, University of California, Santa Barbara, California, USA 5Climate and Environmental Physics, Physics Institute, University of Bern, Bern, Switzerland 6Oeschger Centre for Climate Change Research, University of Bern, Bern, Switzerland Correspondence: Shannon A. Bengtson ([email protected]) Received: 20 May 2020 – Discussion started: 11 June 2020 Revised: 14 December 2020 – Accepted: 15 December 2020 – Published: 25 February 2021 Abstract. The last time in Earth’s history when high lati- 1 Introduction tudes were warmer than during pre-industrial times was the last interglacial period (LIG, 129–116 ka BP). Since the LIG The most recent and well documented warm time period is is the most recent and best documented interglacial, it can the last interglacial period (LIG), which is roughly equivalent provide insights into climate processes in a warmer world. to Marine Isotope Stage (MIS) 5e (Past Interglacials Work- However, some key features of the LIG are not well con- ing Group of PAGES, 2016; Shackleton, 1969). The LIG strained, notably the oceanic circulation and the global car- began at the end of the penultimate deglaciation and ended bon cycle.
    [Show full text]