Periglacial Zone Research Articles

Palaeogeography of South Lithuania during the last ice age

The palaeogeographical development of South Lithuania during the last ice age (Nemunas = Weichselian) was reconstructed by various methods. The recurring permafrost and cryogenic structures in the ground were an important phenomenon of the southeastern periglacial zone. The 3–4 lithocomplexes of the extraglacial cover correlate with the Lithuanian and Mid-European Late Pleistocene Weichselian (Nemunas) biostratigraphic divisions. In the northwest, the palaeogeography is influenced by the deglaciation during the Žiogeliai (Frankfurt) Phase and the Baltija (Pomeranian) Stage of the last ice age. The deglatiation process is shown in a series of palaeogeography maps. During the Weichselian, the SW–NE oriented middle part of the area, commonly regarded as part of the Vilnius-Warsaw-Berlin Urstromtal (ice-marginal streamway), underwent intensive interstadial fluvial erosion and accumulation, glacial erosion and sedimentation, followed by subsequent glaciofluvial accumulation on sandurs and glaciolacustrine sedimentation in a series of small basins.

Depositional environments of the Pleistocene loess-soil series inferred from sand grain morphoscopy—A case study of the East European Plain

Morphoscopy of sand grains from the Late Pleistocene loess–paleosol series exposed on the East European Plain along a longitudinal profile, from the southern limit of the Late Pleistocene ice sheet to the Azov Sea coasts is examined. The data presented refer to three main zones of the loess accumulation different in characteristics of the processes: the northern zone, including the vicinity of the Valdai ice sheet; the middle zone with the maximum sedimentation rate; and the southern zone adjoining seacoasts. The earlier part of the Valdai glacial epoch (before the Bryansk interstadial) was distinct for a rather moderate rate of subaerial processes without any noticeable spatial differentiation with respect to the latitudinal zones. In post-Bryansk time (after ∼24 ka BP) the most active dust accumulation is recorded in the middle zone. The maximum thickness of the Late Pleistocene loess has been recorded there, in the middle reaches of the Dnieper River. In the northern zone the rate of dust settling was not so high, presumably due to high speed of descending winds from the ice sheet. In the southern periglacial zone aeolian abrasion of sand grains was less pronounced as compared with areas farther to the north.

Short-term Periglacial Processes, Vegetation Succession, and Soil Development within Sorted Patterned Ground: Jotunheimen, Norway

Small (1 ≤ m diameter) sorted patterned ground features were studied on the Little Ice Age forelands of three Jotunheimen glaciers. Patterned ground appears to be most active near the ice margins, declining in intensity of activity with distance from the glaciers. Vegetation and soil development are negligible within patterned ground that is “Recent” (decadal time frame). Significant (P < 0.05) fine scale differences in vegetation and soil development occur within patterned ground on terrain ∼70 yr in age, with patterned ground borders having higher values of vegetation cover and thicker soils than that in patterned ground centers. With increasing age of terrain and patterned ground, soil development and vegetation encroach inward toward patterned ground centers, implying that a short-term, active periglacial zone exists near the ice margin, decaying with time and glacier retreat. Specifically, terrain that has been deglaciated for ∼70 years and is approximately ∼350–500 m from the ice margin shows a significant decline in frost activity, allowing for the initiation of pedogenesis and vegetation colonization.

A buoyant life investigating mobile platform (BLIMP)

The search for life in new environments, e.g., Mars/Titan, will be scientifically challenging and have great engineering difficulties. In this paper the authors discuss an approach to field-testing methods relevant to three scientific thrusts in the detection of life and pre-biotic organics on other worlds. We describe how this can be accomplished through a series of field trials using a mobile aerial vehicle that is a proxy for the exploration approaches and instrument techniques necessary for the next stage of life detection on other planets. We do this by deploying a mobile organic laboratory on Earth to demonstrate the requisite techniques. We show how terrestrial field trials provide new insights on the colonization by life of fresh volcanic flows, and the competition between biotic and abiotic processes on a newly cooling piece of the Earth’s crust. This paper suggests that such work could be very effectively conducted on Hawaii, where the erupted lava is basaltic, an important crustal component for terrestrial planets. The presence of water is generally agreed to be a prerequisite for planetary habitability but the combination of basalt and water is chemically unstable at the temperatures to which basalt cools after eruption. The subsequent chemical reactions occur because the total energy of the products is lower than that of the precursor materials and on Earth biological processes result from organisms harvesting that difference in energy. For life processes to succeed they must out-compete the rate at which abiotic chemistry might accomplish the same tasks. Monitoring the rate at which chemical processes occur is therefore a life-detection approach. Biotic involvement in the rate of weathering of basalts is the test case for this new, generic life detection paradigm. This approach would be applicable to the periglacial zones of Mars, if liquid water were proven to be present there. We show that a 15 m autonomous BLIMP could carry various instrument packages including camera, visible spectrometer, tunable diode laser spectrometer (TDLS) for gas and gas isotope analysis, gas chromatograph/mass spectrometer (GCMS). These could be calibrated followed by ground-truthing using field experiments in the interior of Meteor Crater in Arizona. This well understood system could then study the extreme environment of the still active volcanic caldera of Kilauea and the adjacent older lava flows. For Mars the BLIMP is a proxy for a lighter balloon or even a Martian Rover, which could carry a similar suite of instruments and take a similar set of measurements. For Titan, with its dense and high-molecular weight atmosphere calm winds and low gravity, a BLIMP will be the vehicle of choice. The experiments would be directly relevant. We discuss how a Titan BLIMP could search for organic compounds in the post-Cassini exploration of Titan.

Active-Layer Dynamics at the Calypsostranda CALM Site, Recherche Fiord Region, Spitsbergen

Measurements of active-layer thickness were carried out at CALM Site P1 (Calypsostranda), on the southern border of Recherche Fiord (Bellsund region) on the island of Spitsbergen, Svalbard Archipelago. The aim of the studies was to determine the depth and rate of summer thawing and to explain the reasons for local differences. This is of significance owing to the role of the active layer in processes governing development of the periglacial morphogenetic zone. Local factors—including moisture content, vegetation cover, and slope aspect—are important determinants of active-layer thickness and its variability in the Calypsostranda area. Formal sampling and measurement programs, such as those administered by CALM affiliates, are important for discerning between local effects and long-term impacts of climatic changes.

Cryogenic cave calcite from several Central European caves: age, carbon and oxygen isotopes and a genetic model

Cryogenic cave calcite (CCC), formed by segregation of solutes during water freezing, was found in three Central European caves. This calcite type forms accumulations of loose calcite grains on cave floor. The calcite grains are of highly variable crystal morphology, and of sizes ranging from less than 1 mm to over 1 cm. The most typical feature is their accumulation as loose (uncemented) crystals. U-series dating indicates the formation of CCC in the studied caves during several climatic oscillations of the Weichselian (between 61 and 36 ka BP in the Chelsiowa Jama–Jaskinia Jaworznicka cave system in Poland, between 34 and 26 ka BP in the BUML Cave in the Czech Republic, and between 26 and 21 ka BP in the Stratenská Jaskyňa cave system, Slovakia). At the time of CCC formation, the studied caves were lying in a periglacial zone. Detailed C and O stable isotope study of CCC samples revealed that slow water freezing under isotope equilibrium was the dominant formational process in the studied Polish and Czech caves. Significantly higher δ 13C values of CCC in the Stratenská Jaskyňa Cave indicate either water freezing in a more opened system with continuous CO 2 escape (Rayleigh fractional separation), or participation of another CO 2 source. The model of slow water freezing under isotope equilibrium is supported by isolated character of the caves having limited ventilation. In contrast, modern cryogenic cave calcite powders sampled directly on the ice surface of two recently iced caves in Slovakia with high ventilation showed much higher δ 18O and δ 13C data, similar to cryogenic calcites obtained in experimental rapid water freezing.

Formation of patterned ground and fine-scale soil development within two late Holocene glacial chronosequences: Jotunheimen, Norway

Chronosequences of ∼250 to ∼130 years were established on two late Holocene glacier forelands in the Jotunheimen region of southern Norway. Patterned features occurring within chronologically established time units were studied. Young patterned features, forming ∼10–20 years after deglaciation, are frost active. Vegetation cover is minimal within the young patterned features, consisting of bryophytes/organic crusts. Soil development within patterned ground is also minimal/absent because frost action retards horizonization. With time and distance from the glaciated ice margin, frost activity declines within the patterned features, suggesting that a thin, active “periglacial zone” exists near the ice margin. Initially, frost activity decreases at the borders of the features with the centers stabilizing later in time. This results in fine-scale soil heterogeneity and variations of soil development. Fine-scale pedogenic development is first encountered at the borders of patterned ground that has developed on terrain exposed since the ∼1930s, yet soil development is predominantly absent at the centers of patterned ground. With time and distance from the ice margin, frost activity declines and allows patterned features to homogenize from border to center positions in regard to soil characteristics. Across the chronosequences, soils within patterned features pedogenically follow previous soil chronosequence studies, evolving from USDA classifications of Entisols into Inceptisols. Frost disturbance within patterned ground, however, produces a lag effect, that results in longer periods of time for pedogenesis to occur and thinner soils than that of the surrounding terrain.

Evidence for late‐Pleistocene permafrost in the New Jersey Pine Barrens (latitude 39°N), eastern USA

AbstractRelict sand wedges, up to 2.5 m deep and 0.4 m wide, are present in the Pine Barrens of southern New Jersey. They indicate the previous existence of permafrost. The wedges are composed predominantly of sand that shows evidence of wind transport and abrasion. Optically‐stimulated‐luminescence dating of infill material indicates that thermal‐contraction‐cracking and emplacement of the sand infill must have occurred during two separate periods during the Late Pleistocene. The most recent was in Late Wisconsinan times,∼15–18 ka. An earlier period of permafrost conditions is indicated by dates &gt;55–65 ka. On both occasions, the Late‐Pleistocene ice sheets would have advanced as far south as northern New Jersey and strong winds would have occurred in the lower mid‐latitudes. The sandy soils of the Pine Barrens would have allowed the ice‐marginal periglacial zone to extend southwards into southern New Jersey. The sparse tundra vegetation on the sandy substrate, with its relatively high thermal conductivity, would have permitted deep frost penetration because the ‘thermal offset’ would have been minimized. A mean annual air temperature of between −3.0°C and −4.0°C is inferred. Permafrost was probably discontinuous and less than 10–15 m in thickness. Episodes of permafrost thaw are indicated by the widespread occurrence of deformed sediments (‘thermokarst involutions’) and by various small‐scale non‐diastrophic structures associated with bog ironstone beds. The presence of soil (ground) wedges in southern New Jersey and adjacent Delaware also suggest conditions of deep seasonal frost, probably when the most recent permafrost degraded. Copyright © 2003 John Wiley &amp; Sons, Ltd.

Floodplain sedimentation: inherited memories

Swampy inherited floodplains are found throughout the steppe and forest steppe over the Russian Plain. These floodplains were formed during the Late Glacial/Holocene transition on the relicts of large meandering palaeochannels in the former periglacial zone as a result of dramatic decrease in river channel widths (up to 1/15). Inherited floodplains were only partly reworked by the activity of the Holocene rivers. The remnants of the ancient fluvial relief control the flow hydraulics and sediment transport delivery to the river channels on the wide floodplains, causing sediment discontinuity. Such discontinuity reaches its maximum in the chain-of-lakes channels, and decreases with the evolution of the inherited floodplain into a typical floodplain with developed continuous channels.

Fluvial response to the Late Valdai/Holocene environmental change on the East European Plain

The relicts of large meandering paleochannels are found throughout the territory of the periglacial zone of the last (Valdai=Weichselian) glaciation on the Russian Plain, on the lower levels of river terraces and on the floodplains. Channel widths of so-called macromeanders can be 15 times larger than the recent meanders on the same rivers. Paleolandscape and paleohydrological reconstructions show that such periglacial river channels were formed under the conditions of high spring water flow, up to eight times greater than modern discharges, when the flow coefficient was close to 0.9–1.0 due to the existence of permafrost. Also, summers were dry and streams lacked ground water supply. Permafrost degradation increased soil permeability in the spring and increased ground water flow during summer, causing a decrease of annual flow 12,000–14,000 years BP in the southern periglacial zone, and up to 8500 years BP in the northern periglacial zone. In the taiga zone, an annual flow in the recent river basins is about 80–85% of that found in the periglacial zone in the east, and 30–60% of that in the west. In the east of the broad-leaved forest zone, it is about 40–50% of that of the periglacial zone, and 20–25% in the western part of the broad-leaved forest zone. In the eastern steppe and forest steppe, the modern annual flow is about 40–60% of that of the periglacial zone and about 10% in the western part of steppe and forest steppe zones. As a result, large periglacial channels were abandoned and transformed into floodplain lakes and bogs. The Holocene channels have much smaller channel widths and meander lengths, formed under conditions of lower annual flows and much steadier flow regime.

Vistulian loess deposits in western Poland and their palaeoenvironmental implications

The loess deposits of western Poland are a periglacial facies, having been deposited in the Plenivistulian. So far, western Poland is the only part of the country in which Vistulian loess deposits, occurring as small patches on different glacial and glaciofluvial landfoms, have been found. The diagnostic features of these sediments provide a tool for the sub-division of the main lithofacies. Loess deposits occur in two main lithofacies: massive loess (Lm) and laminated loess (Ll). There are three sub-lithofacies within the laminated loess: cryptolaminated (sl), laminated loess sensu stricto (ll) and banded loess (sm). Loess lithofacies are associated with a varied topography and are distributed in the end moraines, till plains and outwash plains. There is a significant correlation with the periglacial zone and aeolian processes active during the Vistulian in western Poland.

THE SO-CALLED URALIC ORIGINAL HOME (URHEIMAT) AND THE SO-CALLED PROTO-URALIC

1. Introductory remarks Following the debate that has been going on over the issue referred to in the title, we can say that the most crucial propositions of Indreko's study have still not been fully answered. (See Indreko 1948, about the origins of Samoyeds and the Saami /Lapp/, the relations between European and Asian cultural centres, the origins of Finno-Ugrians, the issue of original Europeans, the relations between the Mediterranean and periglacial zones /see the arrowheads with a conical edge found in the northern part of the Pyrenees, in the Baltic States and in Central Russia/.) It is a pity that Indreko's splendid study has made so little impact on the research devoted to the Uralic original home during the past 50 years. During the past five years, however, contemporary research on the Uralic original home and the inseparable Proto-Uralic has gained momentum. This positive shift might be attributed to the application of new interdisciplinary approaches, and the greater time depth as opposed to the ones assumed and applied in former linguistic research. 2. The Northern Eurasian Linguistic Zone (NELZ) investigated from linguistic, genetic, anthropological and archaeological aspects There are still several disputes going on concerning the development and the appearance of the earliest anatomically modern human in Europe but we can safely claim that he was present in Europe as early as 35-40 (maybe a bit more) thousand years ago, as there are also traces of him both in the central part of Northern Siberia, and at the lower part of the River Lena. There were some relations to be detected (exchange of goods, intermarriage) among the various communities already in the first phase of the anatomically modern human. On the vast territory, not only genetically and anthropologically different races, but also different cultures and languages developed. Due to the relations between the human communities described above, there might have been some similarities among these races, cultures and languages, while certain regional differences still continued to prevail. Relations between the communities were probably affected by climatic and geographical circumstances. (For instance, during the time of the last European glacial maximum, from 23,000 to 19,500 BC, the land stretching between Fennoscandia and the Alps was uninhabitable. There were some European regions, like Franco-Cantabria and the Dnieper-Don region where refugia were formed. After the glacial maximum people abandoned these refugia and populated the formerly uninhabited parts of Europe such as Northern Europe. During the same period of time, Siberia was not covered with ice.) 2.1. Now let us cite a few examples how these community relations, supposedly lasting for many thousand years, have shaped the linguistic, genetic, anthropological and archaeological character of NELZ. The linguistic situation of Northern Eurasia, irrespective of the genetic classification of languages, seems to exhibit a great deal of similarity (e.g. except for Yenisei languages arriving relatively late in the area, all the dialects belong to the agglutinative-isolating language type, and they likewise show a similar tendency in the linguistic development of local cases and number. In these very categories we can trace other similarities such as identical phonemes K, T, N M, L, applied as local and numeral morphemes, or the omission of P in grammatical functions.) (See more details in e.g. Pusztay 1987, 1990a, 1995.) Genetic research has shown trans-Uralic connections moving from east to west. On the basis of their genofond, Finns do not differ from other Europeans, but the C/T transition appearing in their Y chromosome, which is typical in the Baltic states but is missing as we move on further south, is present in 86% of Yakuts, and 58% of Buryats (Savontaus & Lahermo 1999, Norio 1999). C allele cannot be traced in the central and southern European peoples, but is present among several Northern Asian peoples (the Saami and the Cheremis from the Finno-Ugrian peoples) and therefore it must be originating from Northern Eurasia. …

Channel morphology and river flow in the northern Russian Plain in the Late Glacial and Holocene

The relicts of large meandering palaeochannels are found throughout the territory of the periglacial zone of the Last (Valdai=Weichselian) Glaciation on the Russian Plain. Channel widths of macromeanders can be 15 times larger than the recent meanders of the same rivers. Palaeolandscape and palaeohydrological reconstructions show that these periglacial river channels were formed under conditions of high spring water flow, up to eight times greater than the modern discharges, when the flow coefficient was close to 0.9–1.0 due to presence of permafrost, summers were dry and streams lacked ground water supply. Permafrost degradation increased soil permeability in spring and increased ground water flow in summer, causing a decrease of annual flow (due mainly to the flood flow decrease in spring). As a result, large periglacial channels were abandoned and transformed into lakes and bogs. Late Holocene channels have much smaller channel widths and meander lengths. These were formed under conditions of lower annual flows and much steadier flow regime.

Morfología periglacial del volcán Llullaillaco (Chile/Argentina)

The periglacial processes in the High Andes and resulting periglacial phenomena are presented here by example of Mt. Llullaillaco, at 24°43’ S and 68°32’W, on the frontier between Argentina and Chile. The landforming processes reflect the recent and present extremely arid climate as well as the different age of the volcanics. The range of periglacial landforms, the vertical distribution and association that are described here, result from the interactions of climate and bedrocks. The upper periglacial limits are the highest of the world. The identified phenomena allow to differentiate between the subandine (below 4,100 m), subandine/andine (4,100-4,300 m), andine (4,300-4,700 m), lower periglacial (4,700-5,800 m), medium periglacial (5,800-6,300 m) and upper periglacial (6,300-6,739 m) altitudinal zones. Due to the extreme aridity glaciers cannot form today. Their absence therefore is not due to insufficiently low temperatures, but to lack of humidity.

The European sand belt in eastern Europe ‐ and comparison of Late Glacial dune orientation with GCM simulation results

A compilation is presented of the continuation of the European sand belt, east of Poland. Dune fields encompass most of the aeolian formations in eastern Europe. Supposed sand provenance, dune orientation, and the few available datings suggest initial aeolian activity during cold stages of the Upper‐Pleni (= full)glacial and Late Glacial, similar to northwest and central Europe. Dune fomiation was primarily supply controlled. Comparison of dune orientation with Late Glacial surface wind directions simulated by various GCMs permits reconstruction of dune activation with the positioning of (winter) westerlies over glacial deposits during the Oldest Dryas. Final widespread aeolian activity occurred during the Younger Dryas. As compared to the smaller fields toward the centre of deglaciation, aeolian sand deposits of the intermediate and periglacial zone benefited from distinctly longer intervals of accumulation. In the zone of deglaciation, aeolian activity was restricted to relatively isolated basins.

Late Holocene climatic Forcing of Geomorphic Activity in the Faroe Islands

The location of the Faroe Islands in a climatically uniquely sensitive part of the North Atlantic region provides opportunities to register timing and severity of late Holocene climatic changes reflecting variations in thermohaline circulation. An altitudinal range of 250-450 m a.s.l. represents the modern lower limit for periglacial activity, corresponding to a mean annual air temperature of 5-3.5°C. Above this range, active periglacial features are widespread and plant growth restricted. The periglacial zone extends to the top of the highlands (maximum altitude 882 m a.s.l.). The Iate 20th century climate in the Faroe Islands is characterised by extreme humidity and strong winds, rather than extreme cold. The present treeline is close to sea level, and the potential present discontinuous permafrost level is situated 300-500 m above the highest mountains. Likewise, the modern potential glaciation level is presumably situated only 150-250 m above the highest mountains. During cold intervals of the Little Ice Age the lower limit for periglacial activity may temporarily have approached sea level, simultaneous with incipient establishment of sporadic permafrost in the highlands, and a number of sites in the highest mountains then were presumablyclose to reglaciatíon.

The valdai periglacial zone as an area of cryogenic soil formation

Abstract Stratigraphic successions containing loess, boreal forest palaeosols and cryosols throughout the periglacial area of the Eastern European Plain indicate climate fluctuations throughout the Late Quaternary. Soil development and the genesis of cryogenic features may be contemporaneous (“syneventual”), or pedogenesis may pre-date or post-date cryogenic activity. The Krutitsa (65-54 ka) and Bryansk (32-24 ka) Interstadials were marked by cold and semi-arid continental climates, dominated by open steppe vegetation assemblages. The Bryansk Interstadial was marked by harsher conditions than the earlier Krutitsa. In contrast, colder and extremely arid climates prevailed during the Valdai Glaciation (maximum 20-18 ka), representing the last glacial maximum. Loess deposition and the development of cryogenic features characterized the periglacial areas of the Eastern European Plain. Climate warming, as indicated by the northward recession of the southern limit of permafrost, began ca. 15,000 BP and continued throughout the Younger Dryas and early Holocene, reaching its present position during the Boreal period.

Modalités de la cryoreptation dans les massifs du chambeyron et de la mortice, Haute-Ubaye, Alpes Françaises du sud

From 1975 to 1992, displacements were measured at the soil surface and at depth, at various sites of the Haute-Ubaye, southern French Alps, between 2450 m and 3150 m altitude. The mean rates of movement calculated varied from 0.5 to 5 cm/a. Frost creep predominates; it is more active between 2800 and 3150 m, in the alpine periglacial zone. The fairly elevated silt content of the slope deposits is favourable to frost creep. The evolution of different slopes to produce sorted stripes and solifluction lobes is variable; it depends on vegetation cover, water retention and slope exposure. The movement also varies, yearly, according to the intensity and distribution of precipitation. The soil solifluction is restrained because the number of freezing and thawing cycles is small, generally about 20 to 25 per annum at 5 cm depth.

Gelifluction in the alpine periglacial environment of the Tianshan Mountains, China

AbstractGelifluction in the periglacial zone of the Tianshan Mountains occurs at 2500‐3600 m above sea level on north‐facing slopes. Abundant groundwater, fine grained sediments and slopes 10°‐30° favour gelifluction. Most gelifluction forms are lobate, a few are tongue‐shaped. The mean surface rate of movement is 11.14cm/a; the front advancing rate is 1.86cm/a. The moving rate in the middle part is greater than at the sides of gelifluction lobes, the mean rates being 3.1 cm/a and 0.86cm/a, respectively.

The contemporary periglacial environment in the polar regions

Abstract The present‐day periglacial zones of the polar regions in both hemispheres have many features in common, caused by the peculiarities of climate, glaciological and geocryological processes, and the geomorphology of the periglacial regions. On the other hand, there exist essential differences in the general appearance of the periglacial zones in the Northern and Southern hemispheres, related mainly to particular features of continental glaciation. An analysis of the literature and of data from the author's field observations have allowed him to reach some conclusions as to the major features of the geocryology of the polar regions: the thickness, distribution, temperature, and cryogenic structure of the permafrost and of seasonally frozen materials and the ground ice and cryogenic relief of these areas. This, in turn, made it possible to identify a geocryological zonation of the polar regions and to advance a new concept as to the present‐day periglacial zone.