Eastern Policy of the EU: the Visegrad Countries' Perspective. OSW Point of View, February 2003

1. After its enlargement, scheduled for 2004, the European Union will face a completely new situation at its eastern borders. This new situation calls for a new concept of the EU eastern activities, i.e. for development of the new Eastern Policy of the EU. 2. Due to a number of specific features such as geographical location, closeness of ties, direct risk factors etc., the Visegrad countries will and should be particularly interested in the process of formulating the new EU Eastern Policy. Consequently, they should be the co-makers of this policy. 3. The new EU Eastern Policy should differ fundamentally from the Union's traditional eastern relations. Firstly, its scope should not cover the entire CIS area: instead, the policy should focus on some of the European successor states of the former Soviet Union, namely Belarus, Russia and Ukraine, as well as Moldova, following the accession of Romania. It does not seem advisable to exclude the Russian Federation from this policy and to develop and implement a separate policy towards it. The new Eastern Policy should be an autonomous component and one of the most important elements in the overall foreign policy of the EU. 4. Secondly, the new Eastern Policy should be founded on the following two pillars: a region-oriented strategy, which could be called the Eastern Dimension, and reshaped strategies for individual countries. The Eastern Dimension should set up a universal framework of co-operation, defining its basic mechanisms and objectives. These should include: the adaptation assistance programme, JHA, transborder co-operation, social dialogue and transport infrastructures. The approach, however, should be kept flexible, taking into account the specific situation of each country. This purpose should be served by keeping in place the existing bilateral institutional contacts between the EU and each of its eastern neighbours, and by developing a national strategy for each neighbour.

Wschodnia granica zewnetrzna rozszerzonej Unii Europejskiej. Wspolpraca transgraniczna na nowej granicy wshodniej Unii Europejskiej. Rosyjskojezyczni na Lotwie i w Estonii. Prace OSW 14/2004. The Eastern external border of the enlarge European Union. Cross-border co-operation at the new Eastern border of the European Union. Russian-speakers in Latvia and Estonia. OSW Study 14/2004

Russians or so-called Russian-speakers in Latvia and Estonia pose a significant problem for both countries. Russian-speakers are a numerous minority in Latvia and Estonia, which causes deep division in these countries from the ethnical point of view. The problem of highest importance in the legal aspect is the unregulated status of the Russian-speakers. Though they are permanent residents of Latvia and Estonia many of them still do not have these countries' citizenship. The complex naturalisation procedure introduced by Latvia and Estonia soon after restoring independence in 1991 is considered to be main responsible for this.

Tab. 1: Rates of advance of the frontal push-moraines of 19 lobes in front of an approx. 4.5 km long margin of the Kötlujökull

In the last years masses of ice, about 5 km long, have been protruding from the lowest part of an advancing glacier margin of the Kötlujökull in Southern Iceland. In the summer of 1983, they appeared as sediment-covered lobes, 10-60 m long, bordering the glacier rnargin like agarland. 1 to 3 push-rnoraines without ice core, rnostly sickle-shaped, occured first in the frontal parts of the lobes: behind thern came several ice-cored moraines with heights of up to several metres. The active ice in front of the precipice of the glacier is called the "glacier-foot" in this paper. The digging out of 9 lobes and the measuring of the advance of 19 lobes showed that in most cases this glacierfoot had split up at its distal end into several plate- or stem-shaped pieces of ice which were situated one upon the other, separated by moraine deposits and proceeding irregularly into the foreland at the rate of several mm/h, The sometimes different rate of advance in the same lobe and different rates of advanee in adjoining lobes (some being entirely inactive) point to a type of rnovement which is independent of the general advance of the glacier. Research in the winter of 1983/84 showed less activity in 3 examined lobes, but the activity had not ceased. The advancement of the lower parts of the glacier-foot into and across the sands of the foreland implies the following genesis of pushmoraines: Shoving off a plate of sand, folding it and pushing it over the foreland at average rates of up to 7,2 mm/h, according to the investigations in thc summer of 1983. At a certain stage of the folding process, new folds begin to develop in front of the old, and the old folds are shifted onto the backslope of thc folds in front of them until they are completely unired. In this way, "püe-moraines" arise, which become higher and higher. They include two or more folds declining towards the glacier. Systems of small moraines presumably of the same genesis occur on old moraine areas in front of the Kötlujökull. The possible cause of formation of a glacier-foot is discussed, and the moraines of the Kötlujökull are compared with certain pleistocene push-moraines.

Lithologic, mineral, chemical and isotopic compositions of altered rocks with increasing distance across the eastern flank of the Juan de Fuca Ridge, ODP Leg 168 data

During ODP Leg 168, 10 sites were drilled across the eastern flank of the Juan de Fuca Ridge (JdFR), to examine the conditions of fluid-rock interaction in three distinct hydrothermal regimes (referred to as the Hydrothermal Transition (HT), Buried Basement (BB) and Rough Basement (RB) transects), extending over a ~120 km linear transect perpendicular to the spreading ridge. This was carried out in an attempt to constrain the conditions and processes that control the location, style and magnitude of low temperature (<150°C) fluid-rock interaction within this setting. This paper presents new data on the petrology, mineral chemistry and whole rock strontium and oxygen isotopic compositions of basalts from the eastern flank of the JdFR, in order to investigate the extent, style and sequence of low-temperature hydrothermal alteration and to establish how the hydrothermal regime evolved with time. Throughout the flank, a progressive sequence of low-temperature hydrothermal alteration has been identified, marked by changes in the dominant secondary mineral assemblage, changing from: chlorite+chlorite/smectite; to iron oyxhydroxide+celadonite; to saponite+/-pyrite; culminating at present with Ca- to CaMg(+/-Fe,Mn)-carbonate. The changes in secondary mineralogy have been used to infer a series of systematic shifts in the conditions of alteration that occurred as the basement moved off-axis and was progressively buried by sediment. In general, hydrothermal alteration of the uppermost oceanic crust commenced under open, oxidative conditions, with interaction between unmodified to slightly modified seawater and basaltic crust, to a regime in which circulation of a strongly modified seawater-derived fluid was more restricted, and alteration occurred under non-oxidative conditions. Across the flank, petrological observations and microprobe analyses indicate that the observed ranges in secondary mineral composition are directly related to changes in the geochemical and textural characteristics of the basement, as well as to interaction between fluids and phases from the four stages of alteration. This is suggestive of an increase in fluid-rock increased with time. Whole rock 87Sr/86Sr and d18O analyses of basalts from across the eastern flank of the JdFR reinforce petrological observations, with 87Sr/86Sr and d18O values slightly elevated above accepted pristine MORB values for this region. These results are consistent with an increase in the amount of fluid-rock interaction with time. Across the flank, enrichment in the 87Sr/86Sr and d18O relative to MORB, is influenced by a number of factors, including: local and regional variations in the crustal lithology and structure; the age of the crust; the extent of bulk rock alteration; and theoretically, the relative abundance of different isotopically-enriched secondary mineral phases in the crust.

(Table 1) Age determination of sediment cores of the Labrador Sea

A close look at the sedimentology of Heinrich event 4 from the northwest Labrador Sea indicates that an extended ice margin, perhaps greater than before Heinrich events 1 or 2 (H-1 and H-2), existed in the Hudson Strait region pre-Heinrich event 4 (H-4) and, that on the basis of characteristics of the sediment unit, Heinrich event-4 was different than Heinrich events 1 or 2 (i.e., larger ice sheet collapse(?), longer duration(?), "dirtier" icebergs(?)). Other data from across the southern and eastern margin of the Laurentide Ice Sheet, as well as Greenland and the North Atlantic, support this interpretation, possibly indicating a relative mid-Wisconsin glacial maximum pre-Heinrich event 4. Many of these data also indicate that Heinrich event 4 (35 ka) resulted in serious climatic and oceanographic reorganizations. We suggest that Heinrich event 4 gutted the Hudson Strait, leaving it devoid of ice for Heinrich event 3. We further hypothesize that Heinrich event 3 did not originate from axial ice transport along the Hudson Strait; thus Heinrich event 3 may be more analogous to the proposed northward advancing ice from Ungava Bay during Heinrich event 0 than to the more typical down-the-strait flow during H-1, H-2, and H-4. Consequently, the climatic and oceanographic impacts resulting from Heinrich events are highly susceptible to the type, origin, and magnitude of ice sheet collapse, something which varied per Heinrich event during the last glacial period.

Geology along the southern margin of the Absaroka range, Wyoming.

Mode of access: Internet.

Report of the Commissioners upon the erection of the new hospital for the insane, in the north-eastern part of the commonwealth. 1876.

Mode of access: Internet.