Counter Strike – Global Offensive ESK Kosova
Counter Strike – Global Offensive-ESK Kosova
Now you have the opportunity to download (download) Counter Strike – Global Offenisve ESK, this is edit special for Albanian players from Hajrullah Makolli.
This game is about 2.80 verison Giga Byte is not too big for your PC so you can very easily download it.
This version of the game features the Update, which works if you do not play can make Update
Graphic for this game :
OS: Windows 7/Vista/XP
CPU: Intel Core™ 2 Duo E6600 or AMD Phenom™ X3 8750 processor or better
RAM: 1GB XP / 2GB Vista
HDD: At least 7.6GB of Space
GPU: Video card must be 256 MB or more and should be a DirectX 9-compatible with support for Pixel Shader 3.0
You can change name:
For 32 Bit Users: C:\Program Files\Counter-Strike Global Offensive eSK\rev.ini
(edit find or ctrl+f search hajrullah replace hajrullah with your desired nickname)
For 64 Bit Users: C:\Program Files (x86)\Counter-Strike Global Offensive eSK\rev.ini
(edit find or ctrl+f search hajrullah replace hajrullah with your desired nickname)
IP : 220.127.116.11:27015 | Kosovo Server | Global Offensive
Link for download :
Direct Link : Global Offensive ESK
One of the oldest known ball games in history is the Mesoamerican ballgame (Ōllamaliztli in Nahuatl). Ōllamaliztli was played as far back as 1,400 BC and had important religious significance for the mesoamerican peoples such as the Maya and Aztec. The game evolved over time but the main goal was to keep a solid rubber ball in play by striking it with various parts of the body or with tools such as rackets. The game may have served as a proxy for warfare and also had a major religious function. Formal ballgames were held as ritual events, often featuring human sacrifice, though it was also played for leisure by children and even women.
The indigenous North American peoples played various kinds of stickball games, which are the ancestors of modern Lacrosse. Traditional stickball games were sometimes major events that could last several days. As many as 100 to 1,000 men from opposing villages or tribes would participate. The games were played in open plains located between villages, and the goals could range from 500 yards (460 m) to 6 miles (9.7 km) apart.
The Tafl games were a family of ancient Germanic and Celtic board games played across much of Northern Europe from earlier than 400 CE until the 12th century. Although the rules of the games were never explicitly recorded, it seems to have been a game with uneven forces (2:1 ratio) and the goal of one side was to escape to the side of the board with a King while the other side’s goal was to capture him. Tafl was spread by the Vikings throughout northern Europe, including Iceland, Britain, Ireland, and Lapland.
Chess was introduced to the Iberian emirate of Cordoba in 822 during the reign of Abd ar-Rahman II. By the middle of the 10th century it was being played in Christian Spain, Italy and Southern Germany. By 1200, it had reached Britain and Scandinavia. Initially there were many differing local Chess games with varying rules or assizes such as Short assize chess, Courier chess and Dice Chess.
An important source of medieval games is the Libro de los juegos, (“Book of games”), or Libro de acedrex, dados e tablas, (“Book of chess, dice and tables”, in Old Spanish) which was commissioned by Alfonso X of Castile, Galicia and León in 1283. The manuscript contains descriptions and color illustrations of Dice games, Chess and tabula, a predecessor of Backgammon. The book portrays these games within an astrological context, and some game variants are astronomically designed, such as a game titled “astronomical chess”, played on a board of seven concentric circles, divided radially into twelve areas, each associated with a constellation of the Zodiac. The symbolism of the text indicates that some of these games were given metaphysical significance. Chess was also used to teach social and moral lessons by the Dominican monk Jacobus de Cessolis in his Liber de moribus hominum et officiis nobilium super ludo scacchorum (‘Book of the customs of men and the duties of nobles or the Book of Chess’). Published circa 1300, the book was immensely popular.
Other pre-modern European board games include Rithmomachy or “the philosophers game”, Alquerque, Fox & Geese, Nine Men’s Morris, Draughts, Nim, Catch the Hare and the Game of the Goose. Dice games were widely played throughout Europe and included Hazard, Chuck-a-luck, Glückshaus, Shut the Box and knucklebones.
Card games first arrived in Italy from Mamluk Egypt in the 14th century, with suits very similar to the Swords, Clubs, Cups and Coins and those still used in traditional Italian and Spanish decks. The four suits most commonly encountered today (spades, hearts, diamonds, and clubs) appear to have originated in France circa 1480. 1440s Italy saw the rise of tarot cards and this led to the development of Tarot card games such as Tarocchini, Königrufen and French tarot. The decks were also sometimes used for cartomancy.
Outdoor games were very popular during holidays and fairs and were played by all classes. Many of these games are the predecessors of modern sports and lawn games. Boules, Lawn Billiards (later brought indoors as Billiards), Skittles (an ancestor of modern ten pin Bowling), medieval football, Kolven, Stoolball (an ancestor of Cricket), Jeu de paume (early racket-less tennis), Horseshoes and Quoits all predate the early modern era.
Modern chess rules began taking shape in Spain and Italy during the 15th century with the adoption of the standard Queen and Bishop movements (initially called “Mad Queen chess”). Writings on chess theory also began to appear in the 15th century with the first text being the Repetición de Amores y Arte de Ajedrez (Repetition of Love and the Art of Playing Chess, 1497) by Spanish churchman Luis Ramirez de Lucena. Chess books by authors such as Ruy López de Segura and Gioachino Greco became widely studied. Chess was the favored game of Voltaire, Rousseau, Benjamin Franklin and Napoleon.
In 1851, the first international chess tournament was held in London and won by Adolf Anderssen. Soon after modern time control rules were adopted for competitive play. The first Official World Chess Championship was held in 1886 in the United States and won by Wilhelm Steinitz. By the 20th century, the game of Chess had developed into a professional sport with chess clubs, publications, player ratings and chess tournaments. The World Chess Federation (FIDE) was founded in 1924 in Paris.
A large number of Chess variants were also developed, with varying pieces, rules, boards and scoring. Among them are Kriegspiel, Capablanca Chess, Alice Chess, Circular chess, Three-dimensional chess, Hexagonal Chess, Chess with different armies, and Bobby Fischer’s Chess960.
In Japan, Go and Shogi became the major board games played at a professional level. Both games were promoted in Japan by the Tokugawa shogunate in the 17th century, and top players (Meijin) received government endowments. During the 20th century the Japan Shogi Association and the Japan Go Association were founded and began organizing professional tournaments. During the Qing dynasty, many Xiangqi clubs were formed and books published. The Chinese Xiangqi Association was formed in 1962, and Xiangqi tournaments are held worldwide by national Xiangqi associations.
In 1997 the first Mind Sports Olympiad was held in London and included traditional as well as modern board games. Other board games such as Backgammon, Scrabble and Risk are also played professionally with dedicated world championships.
Look photo :
he total surface area of the Earth is about 510 million km2 (197 million sq mi). Of this, 70.8%, or 361.13 million km2 (139.43 million sq mi), is below sea level and covered by ocean water. Below the ocean’s surface are much of the continental shelf, mountains, volcanoes, oceanic trenches, submarine canyons, oceanic plateaus, abyssal plains, and a globe-spanning mid-ocean ridge system. The remaining 29.2% (148.94 million km2, or 57.51 million sq mi) not covered by water has terrain that varies greatly from place to place and consists of mountains, deserts, plains, plateaus, and other landforms. Tectonics and erosion, volcanic eruptions, flooding, weathering, glaciation, the growth of coral reefs, and meteorite impacts are among the processes that constantly reshaping and have reshaped the Earth’s surface over geological time.
The continental crust consists of lower density material such as the igneous rocks granite and andesite. Less common is basalt, a denser volcanic rock that is the primary constituent of the ocean floors. Sedimentary rock is formed from the accumulation of sediment that becomes buried and compacted together. Nearly 75% of the continental surfaces are covered by sedimentary rocks, although they form about 5% of the crust. The third form of rock material found on Earth is metamorphic rock, which is created from the transformation of pre-existing rock types through high pressures, high temperatures, or both. The most abundant silicate minerals on Earth’s surface include quartz, feldspars, amphibole, mica, pyroxene and olivine. Common carbonate minerals include calcite (found in limestone) and dolomite.
The elevation of the land surface varies from the low point of −418 m at the Dead Sea, to a maximum altitude of 8,848 m at the top of Mount Everest. The mean height of land above sea level is 840 m.
The pedosphere is the outermost layer of Earth’s continental surface and is composed of soil and subject to soil formation processes. The total arable land is 10.9% of the land surface, with 1.3% being permanent cropland. Close to 40% of Earth’s land surface is used for cropland and pasture, or an estimated 1.3×107 km2 of cropland and 3.4×107 km2 of pastureland.
The abundance of water on Earth’s surface is a unique feature that distinguishes the “Blue Planet” from other planets in the Solar System. Earth’s hydrosphere consists chiefly of the oceans, but technically includes all water surfaces in the world, including inland seas, lakes, rivers, and underground waters down to a depth of 2,000 m. The deepest underwater location is Challenger Deep of the Mariana Trench in the Pacific Ocean with a depth of 10,911.4 m.[n 19]
The mass of the oceans is approximately 1.35×1018 metric tons, or about 1/4400 of Earth’s total mass. The oceans cover an area of 3.618×108 km2 with a mean depth of 3682 m, resulting in an estimated volume of 1.332×109 km3. If all of Earth’s crustal surface was at the same elevation as a smooth sphere, the depth of the resulting world ocean would be 2.7 to 2.8 km.
About 97.5% of the water is saline; the remaining 2.5% is fresh water. Most fresh water, about 68.7%, is present as ice in ice caps and glaciers.
The average salinity of Earth’s oceans is about 35 grams of salt per kilogram of sea water (3.5% salt). Most of this salt was released from volcanic activity or extracted from cool igneous rocks. The oceans are also a reservoir of dissolved atmospheric gases, which are essential for the survival of many aquatic life forms. Sea water has an important influence on the world’s climate, with the oceans acting as a large heat reservoir. Shifts in the oceanic temperature distribution can cause significant weather shifts, such as the El Niño-Southern Oscillation.
The atmospheric pressure on Earth’s surface averages 101.325 kPa, with a scale height of about 8.5 km. It has a composition of 78% nitrogen and 21% oxygen, with trace amounts of water vapor, carbon dioxide and other gaseous molecules. The height of the troposphere varies with latitude, ranging between 8 km at the poles to 17 km at the equator, with some variation resulting from weather and seasonal factors.
Earth’s biosphere has significantly altered its atmosphere. Oxygenic photosynthesis evolved 2.7 Gya, forming the primarily nitrogen–oxygen atmosphere of today. This change enabled the proliferation of aerobic organisms and, indirectly, the formation of the ozone layer due to the subsequent conversion of atmospheric O2 into O3. The ozone layer blocks ultraviolet solar radiation, permitting life on land. Other atmospheric functions important to life include transporting water vapor, providing useful gases, causing small meteors to burn up before they strike the surface, and moderating temperature. This last phenomenon is known as the greenhouse effect: trace molecules within the atmosphere serve to capture thermal energy emitted from the ground, thereby raising the average temperature. Water vapor, carbon dioxide, methane and ozone are the primary greenhouse gases in the atmosphere. Without this heat-retention effect, the average surface temperature would be −18 °C, in contrast to the current +15 °C, and life would likely not exist.
Earth’s atmosphere has no definite boundary, slowly becoming thinner and fading into outer space. Three-quarters of the atmosphere’s mass is contained within the first 11 km of the surface. This lowest layer is called the troposphere. Energy from the Sun heats this layer, and the surface below, causing expansion of the air. This lower-density air then rises, and is replaced by cooler, higher-density air. The result is atmospheric circulation that drives the weather and climate through redistribution of thermal energy.
The primary atmospheric circulation bands consist of the trade winds in the equatorial region below 30° latitude and the westerlies in the mid-latitudes between 30° and 60°. Ocean currents are also important factors in determining climate, particularly the thermohaline circulation that distributes thermal energy from the equatorial oceans to the polar regions.
Water vapor generated through surface evaporation is transported by circulatory patterns in the atmosphere. When atmospheric conditions permit an uplift of warm, humid air, this water condenses and falls to the surface as precipitation. Most of the water is then transported to lower elevations by river systems and usually returned to the oceans or deposited into lakes. This water cycle is a vital mechanism for supporting life on land, and is a primary factor in the erosion of surface features over geological periods. Precipitation patterns vary widely, ranging from several meters of water per year to less than a millimeter. Atmospheric circulation, topographic features and temperature differences determine the average precipitation that falls in each region.
The amount of solar energy reaching Earth’s surface decreases with increasing latitude. At higher latitudes the sunlight reaches the surface at lower angles and it must pass through thicker columns of the atmosphere. As a result, the mean annual air temperature at sea level decreases by about 0.4 °C (0.7 °F) per degree of latitude from the equator. Earth’s surface can be subdivided into specific latitudinal belts of approximately homogeneous climate. Ranging from the equator to the polar regions, these are the tropical (or equatorial), subtropical, temperate and polar climates. Climate can also be classified based on the temperature and precipitation, with the climate regions characterized by fairly uniform air masses. The commonly used Köppen climate classification system (as modified by Wladimir Köppen’s student Rudolph Geiger) has five broad groups (humid tropics, arid, humid middle latitudes, continental and cold polar), which are further divided into more specific subtypes.
Climate on Earth has latitudinal anomalies, namely the habitability of the Scandinavian peninsula very far north in sharp contrast to the polar climates of northern Canada as well as the cool summers expected at low latitudes in the Southern Hemisphere (for example on the west coast of South America). Another anomaly is the impact of landmass on temperature, manifested by the fact that Earth is much warmer at aphelion, where the planet is at a more distant position from the Sun. When the Northern hemisphere is turned towards the sunlight even the increased distance to it does not hinder temperatures to be 2.3 °C (4 °F) warmer than at perihelion—when the marine southern hemisphere is turned towards the Sun.
At high latitudes, the western sides of continents tend to be milder than the eastern sides—for example seen in North America and Western Europe where rough continental climates appear on the east coast on parallels with mild climates on the other side of the ocean.
The highest air temperature ever measured on Earth was 56.7 °C (134.1 °F) in Furnace Creek, California, in Death Valley, in 1913. The lowest air temperature ever directly measured on Earth was −89.2 °C (−128.6 °F) at Vostok Station in 1983, but satellites have used remote sensing to measure temperatures as low as −94.7 °C (−138.5 °F) in East Antarctica. These temperature records are only measurements made with modern instruments from the 20th century onwards and likely do not reflect the full range of temperature on Earth.