scholarly journals PERIOD OF INTENSE VEGETATION IN POLAND IN THE YEARS 1966–2015

1970 ◽  
pp. 239-248
Author(s):  
Arkadiusz M. Tomczyk ◽  
Katarzyna Szyga–Pluta
Keyword(s):  
Air Temperature ◽  
Vegetation Period ◽  
Longitudinal Distribution ◽  
The South ◽  
The West ◽  
Start Date ◽  
North East ◽  
The North ◽  
South West ◽  
Mathematical Formulas

The purpose of this paper was to determine long-range and spatial variability of the start and end dates of a period of intense vegetation in Poland in 1966–2015. The article is based on average monthly air temperature values acquired for 20 Polish stations for 1966–2015, made available by the Institute of Meteorology and Water Management – the National Research Institute. Based on the obtained data, the dates of the beginning and end of the intense vegetation period were determined. In this study, the intense vegetation period was defined as one with an average daily air temperature ≥10°C. The mathematical formulas proposed by Gumiński (1948) were used to determine the dates of the beginning and end of the period. A period of intense vegetation in Poland in the years 1966–2015 has extended. The dates of the beginning of the period of intense vegetation changed in the latitudinal system from the south to the north while the intensity of changes in the date of the beginning in the studied area was characterized by longitudinal distribution – the most prominent in the west of Poland. The end of the intense vegetation period occurs earliest in the north-east of Poland, and latest in the west and the south. The end date changes were less significant than the start date changes. The length of the intense vegetation period ranges from the north-east to the south-west of Poland, and the most dramatic changes occurred in the west and the south-east of Poland.

The West Court at Perachora

1967 ◽  
Vol 62 ◽  
pp. 353-371
Author(s):  
J. J. Coulton
Keyword(s):  
Short Distance ◽  
Sixth Century ◽  
East Side ◽  
The South ◽  
The West ◽  
Rock Face ◽  
North East ◽  
The North ◽  
South West ◽  
East And West

About 10 metres south-west of the sixth-century temple of Hera Akraia at Perachora, and nearly due west of the little harbour lies the small courtyard previously known as the ‘Agora’. Since its purpose is not known, it will here be non-committally referred to as the West Court. It was first excavated in 1932, and more fully, under the supervision of J. K. Brock, in 1933, but it was not entirely cleared until 1939, and it was at that time that the Roman house which stood in the middle of the court was demolished. The West Court is discussed briefly (under the name of ‘Agora’) in Perachora 1 and in the preliminary reports of the Perachora excavations. Short supplementary excavations were carried out in 1964 and 1966 to examine certain points of the structure.In shape the West Court is an irregular pentagon, about 24 metres from north to south and the same from east to west (Fig. 1; Plate 91 a, b). It is enclosed on the west, north, and on part, at least, of the east side by a wall of orthostates on an ashlar foundation. For a short distance on either side of the south corner, the court is bounded by a vertically dressed rock face which is extended to the north-east and west by walls of polygonal masonry. At the south-west corner the west orthostate wall butts against the polygonal wall, which continues for about 0·80 m. beyond it and then returns north for about 8 metres behind it.

scholarly journals An ultrabasic pipe in the eastern Sukkertoppen region, southern West Greenland

1980 ◽  
Vol 100 ◽  
pp. 69-73
Author(s):  
R.P Hall
Keyword(s):  
Granulite Facies ◽  
The South ◽  
The West ◽  
West Side ◽  
West Greenland ◽  
North East ◽  
The North ◽  
South West ◽  
Unusual Occurrence ◽  
Anorthosite Complex

An unusual occurrence of ultrabasic material was located in the eastern Sukkertoppen region during the reconnaissance mapping programme of 1977, the findings of which were described by Allaart et al. (1978). It occurs on a small exposure on the west side of a north-pointing peninsula in the middle of the large nunatak Majorqap alangua (65°53'N, 50°40'W), to the north-east of the Majorqaq valley (Hall, 1978, fig. 21). The area is composed predominantly of a suite of granulite facies granitic gneisses which contain numerous enclaves of pyroxene-bearing amphibolites, and locally anorthositic and gabbroic rocks similar to those seen in the Fiskenæsset anorthosite complex (Myers, 1975). The gneisses in the centre af the nunatak are highly irregular in orient at ion, occupying the complex interseclion af closures af at least two major fold phases. A belt af amphibolitcs forms the cliff at the south-west tip af Majorqap alangua. Related rocks occur in arnphibolite facies in the acea around the lakc Qardlit taserssuat immediately to the soulh (Hall, 1978).

scholarly journals Results from a geological reconnaissance around Svartenhuk Halvø, West Greenland

1973 ◽  
Vol 50 ◽  
pp. 1-26
Author(s):  
V Münther
Keyword(s):  
Fault Zones ◽  
The South ◽  
Large Area ◽  
The West ◽  
North East ◽  
The North ◽  
South West ◽  
Early Tertiary ◽  
Lateral Extent ◽  
Tectonic Movements

Svartenhuk Halvø is built up primarily of Tertiary basalts; these overlie Cretaceous and early Tertiary sediments, and overlap onto the Precambrian basement. The basalt series can be divided into a lower and an upper series; although displaced by faults, the boundary between these series can be followed across the peninsula. The thickness of the lower basalt series is estimated to be about 2-3 km in the south of the peninsula and barely 1 km in the north; the sub-aquatic basalt breccia is included in these thicknesses. FauIts causing repetitions of the lava succession have resulted in the series being preserved over a rather large area. The general dip of the lavas is 3-4 dregrees towards SW in the east and 8-10 degrees, also towards SW, in the west. Locally dips between 10 and 20 degrees or even steeper are seen; these are the resulf of drag along fault zones in Arfertuarssuk fjord and Kugssineq valley, and between Svartenhuk Halvø and Ubekendt Ejland. The youngest fault has a displacement of 500 m or more and has downthrown the basement area to the north-east in relation to the sediment-basalt breccia-basalt series to the south-west. The upper basalt series has by far the greater lateral extent and covers the gneiss and metasediment area to the north and north-east at least as far as the Inland lee. The dip of the flows in this part of the basalt series is considerably lower than in much of the lower basalt series, but faults repeating the succession are also frequently encountered within the upper basalts. The tectonic movements evidence a strong E-W (or NE-SW) tension, never a compression; the weak anticlinal and synclinal structures which are seen are interpreted as resulfing from differential sagging. The lower basalt series is thought to have arisen from fissure eruptions, with the main area of eruption in the east. The lavas are very rich in olivine (i. e. are pieritic). The upper basalt series probably arose from central eruptions and smaller fissure eruptions, and the area of eruption is thought to have shifted to the west. The upper lavas become poorer in olivine; andesitic lavas represent perhaps a closing phase, more local in its distribution and perhaps resulting from magmatic assimilation of pre-basaltic sediments. "Iron basalt" and intrabasaltic breccia have not been noted on Svartenhuk Halvø.

GEOLOGY OF THE NORTH-EAST MARGIN OF THE GREAT ARTESIAN BASIN QUEENSLAND, AUSTRALIA

1965 ◽  
Vol 5 (1) ◽  
pp. 179
Author(s):  
Edward F. Durkee
Keyword(s):  
Sedimentary Rocks ◽  
The South ◽  
The West ◽  
Artesian Basin ◽  
Late Mesozoic ◽  
Great Artesian Basin ◽  
North East ◽  
The North ◽  
South West ◽  
Basin Margin

The north-east margin of the basin as described herein comprises some 40,000 square miles situated regionally between the Bowen basin and the Drummond Range on the east and north-east respectively and the towns of Longreach, Charleville, and Mitchell on the west and south. The limit of the present-day Great Artesian basin in this area is marked by south-east striking outcrops of the Jurassic Precipice Sandstone.The stratigraphy of the area can be grossly subdivided into three time-rock units as follows:Pre-PermianPermian-TriassicLate Mesozoic and Tertiary.Pre-Permian rocks of importance include thick Devonian and Carboniferous units. Marine and evaporite facies are present in the Devonian in the south-west (Adavale basin), changing to more continental facies with volcanic and some marine incursions to the north-east (Drummond basin). Carboniferous units are dominantly paralic to continental types. The Devonian and Carboniferous systems were subjected to various degrees of pre-Permian tectonism and removal and, because of this, the existing occurrences of these systems are only fragments of their original extent. Permian and Triassic, marine to continental units were deposited across the area, thinning from east to west in possible cycles of transgression and regression. In addition to thinning regionally, these systems show marked variation in thickness due to transgression and drape and compaction over major, pre-Permian structural trends.Subsequent to deposition of the Triassic, a pronounced tectonic change was introduced. Previously negative areas to the north-east (Drummond basin—Springsure Shelf) began to rise and the Middle to Late Mesozoic subsidence and filling of the Great Artesian basin to the south-west commenced. Therefore, Triassic and Permian strata thicken regionally to the north-east under the Great Artesian basin margin, while post-Triassic strata thicken south-westward, in the opposite direction, into the basin.Three dominant structural trends are reflected in the sedimentary rocks of the area. These are:North-east trends under much of the Great Artesian basin margin.North-westerly trends of the Drummond basin to the north-east of the Great Artesian basin margin.Northern trends of the Denison trough east of the Great Artesian basin margin.

2. The Surface Geology of Mid-Lochaber

1882 ◽  
Vol 11 ◽  
pp. 483-487
Author(s):  
Duns
Keyword(s):  
Point Of View ◽  
The Body ◽  
The South ◽  
The West ◽  
North East ◽  
The North ◽  
South West ◽  
Surface Geology ◽  
Made In

An attempt is made in this paper, mainly from the point of view of the Society's “Boulder Committee,” to examine and classify the surface-deposits of a comparatively small compact area, which is bounded on the north and north-east by the river Spean, on the south and south-west by the river Nevis, on the west and northwest by the Lochy and the Caledonian Canal, and on the east and south-east by the Nevis range of Mountains. Reference is also made to the district between the Nevis and Loch Linnhe, including Auchintore and part of Glen Nevis. The body of the paper is limited to the statement of phenomena. It is felt, however, that the chief value of a record of facts is to lead to a definite knowledge of the forces which underlie them, and of the laws of which they are the expression.

Hadd Hajar, a clausura in the Tripolitanian Gebel Garian south of Asabaa

1980 ◽  
Vol 11 ◽  
pp. 45-52 ◽  
Author(s):  
Olwen Brogan
Keyword(s):  
Sea Level ◽  
East Side ◽  
The South ◽  
The West ◽  
North East ◽  
The North ◽  
South West ◽  
Narrow Valley ◽  
Pass Through ◽  
The Hill

In the Gebel Garian, about 20 kilometres south of Asabaa, the map-makers of 1964 indicated an ancient wall (Fig. 1) called Hadd Hajar (i.e. wall of stone) running south-west for six kilometres from Ras al Tays al Abyad (858 m; the Hill of the White Goat) on which stood a watch tower, to Ras al Said (764 m). The country crossed by Hadd Hajar is about 690-730 m above sea-level with a gently-undulating surface constituting a fairly open and level valley. The hills are covered with esparto-grass. On the west the Wadi Wamis winds among closely-set hills while, in the north-east, the wall is carried for a further three quarters of a kilometre across a narrow valley from Ras al Tays al Abyad to another hill Ras al Saqifah. An old track comes southwards down this valley flanked on the east side by a barrier of hills over 800 m high. Where the track crosses the wall there is a Roman building (Gasr al Saqifah) with traces of an archway for people and flocks to pass through. Two kilometres to the south is an old cistern (Majin Saqifah) presumably Roman. Beyond, the track continues about 25 kilometres to a large well, Bir al Shaqaykah (Sceghega), after which it is another 28 kilometres south-eastwards to Mizdah on the Wadi Sofeggin.

scholarly journals The Igneous Complex of Y Foel Fras, Caernarvonshire

1922 ◽  
Vol 59 (3) ◽  
pp. 134-139 ◽  
Author(s):  
Norman L. Silvester
Keyword(s):  
Coastal Plain ◽  
Geological Survey ◽  
The South ◽  
The West ◽  
Igneous Complex ◽  
North West ◽  
North East ◽  
The North ◽  
South West

The area under consideration is a portion of the mountain massif bounded on the east by the Conway River, on the north by the narrow coastal plain between Conway and Bangor, and on the west and south by the popular tourist route through Nant.-Francon pass by Llyn Ogwen and down the Afon Llugwy to Bettws y coed. The investigation includes the horseshoe-shaped ring of mountains, of which the highest is Y Foel Frâs (3,091 feet), surrounding the upper course of the Aber River (Cwm yr Afon Goch). To the north-west this igneous complex is bounded by the precipitatious crags over which the above stream descends by leaps and bounds, forming the well-known Aber Falls. Upon Sheet 78, south-east of the old Geological Survey map the area is coloured as “Massive intrusive felspathic rocks”, surrounding two oval patches indicated as “Greenstones”, whilst a further elongated patch of the latter forms the south-west boundary. The north-east boundary is limited by the Aber-Llanbedr fault. Besides the hog-backed summit of Y Foel Frâs, the area includes the similarly outlined summits of Y Drosgl West (2,483 feet), Yr Arryg (2,875 feet), Llwydmor Bâch (2,256 feet), and the more rugged summits of Bera Mawr (2,587 feet), Bera Bâch and Llwydmor (2,749 feet).

The Metamorphosed Limestones and Associated Contaminated Igneous Rocks of the Carlingford District, Co. Louth

1932 ◽  
Vol 69 (5) ◽  
pp. 209-233 ◽  
Author(s):  
G. D. Osborne
Keyword(s):  
Igneous Rocks ◽  
The South ◽  
Ordnance Survey ◽  
Igneous Complex ◽  
North East ◽  
The North ◽  
South West ◽  
Carboniferous Limestone ◽  
Contamination Effects

THE Carlingford-Barnave district falls within the boundaries of Sheet 71 of the Ordnance Survey of Ireland, and forms part of a broad promontory lying between Carlingford Lough on the north-east and Dundalk Bay on the south-west. The greater part of this promontory is made up of an igneous complex of Tertiary age which has invaded the Silurian slates and quartzites and the Carboniferous Limestone Series. This complex has not yet been investigated in detail, but for the purposes of the present paper certain references to it are necessary, and these are made below. The prevalence of hybrid-relations and contamination-effects between the basic and acid igneous rocks of the region is a very marked feature, and because of this it has been difficult at times to decide which types have been responsible for the various stages of the metamorphism.

scholarly journals The Results of a Chemical, Microscopical and Bacteriological Examination of Samples of London Milks

1907 ◽  
Vol 7 (1) ◽  
pp. 22-31 ◽  
Author(s):  
R. Tanner Hewlett ◽  
George S. Barton
Keyword(s):  
Bacteriological Examination ◽  
Milk Supply ◽  
The South ◽  
The West ◽  
The North ◽  
South West ◽  
Pure Milk

In view of the importance of a pure milk supply, we considered that it might be of interest to examine chemically, microscopically, and bacteriologically, a number of specimens of milk coming into the Metropolis for which purpose we decided to select samples from the various counties, the milk of which is consigned to London. We found that milk so consigned comes from about twenty-six counties extending from Derby in the North, to Hampshire and Devonshire in the South and South-West, and from Hereford in the West, to Norfolk in the East.

Part VI. The Cyclopean Terrace Building and the Deposit of Pottery beneath It

1954 ◽  
Vol 49 ◽  
pp. 267-291
Author(s):  
Elizabeth B. Wace
Keyword(s):  
Contour Line ◽  
The South ◽  
Main Road ◽  
North West ◽  
North East ◽  
The North ◽  
South West

The Cyclopean Terrace Building lies to the north-west of the Lion Gate on the northern end of the Panagia Ridge and faces almost due west across the valley of the Kephissos and modern main road from Corinth to Argos. It lies just below the 200 m. contour line, and one terrace below the houses excavated in 1950–51 by Dr. Papadimitriou and Mr. Petsas to the east at the same end of the ridge. The area contains a complex of buildings, both successive and contemporary, and in view of the discovery of structures both to the south-west and, by the Greek Archaeological Service, to the north-east it is likely that this whole slope was covered by a portion of the outer town of Mycenae. This report will deal only with the structure to which the name Cyclopean Terrace Building was originally given, the so-called ‘North Megaron’, supported by the heavy main terrace wall.The excavation of this structure was begun in 1923. The main terrace wall was cleared and two L.H. IIIC burials discovered in the top of the fill in the south room. In 1950 it was decided to attempt to clear this building entirely in an endeavour to find out its date and purpose. The clearing was not, however, substantially completed until the close of the 1953 excavation season, and this report presents the available evidence for the date as determined by the pottery found beneath the building; the purpose is still a matter for study, though various tentative conclusions can be put forward.

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