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Water {Oceans}
I. The Hydrological (Water) Cycle
Definition and Process
• The hydrological cycle explains how water moves on, in, and above Earth.
• Water continuously circulates between the oceans, land, the atmosphere, and living organisms.
• This cycle has been operating for billions of years and is essential for all life.States of Water
• Water exists in three forms:
– Liquid: Water in oceans, lakes, streams, and groundwater.
– Solid: Ice found in glaciers and icecaps.
– Gas: Water vapor present in the atmosphere.Distribution of Water
• About 71% of Earth’s water is found in the oceans.
• The remaining water exists as freshwater in glaciers, icecaps, groundwater, lakes, soil moisture, streams, the atmosphere, and within living organisms.
• Nearly 59% of water falling on land returns to the atmosphere via evaporation (from both oceans and other surfaces); the rest becomes runoff, infiltrates the ground, or accumulates as glaciers.Importance and Challenges
• Water is vital for life, second only to air.
• Earth is unique in having an abundant water supply, which is why it’s called the “Blue Planet.”
• Although the total amount of renewable water remains constant, increasing demand and pollution (especially of river water) have led to water crises that vary by region and time.
II. Relief (Physical Features) of the Ocean Floor
General Characteristics
• The ocean floor is the “land” beneath the seas and shows varied features similar to those on continents.
• Most of the ocean floor lies between 3 and 6 km below sea level.
• These features are created by tectonic movements, volcanic activity, and the deposition of sediments.Division of the World’s Oceans
• The Earth’s oceanic parts are divided into five main oceans:
– Pacific
– Atlantic
– Indian
– Southern
– Arctic
• Seas, bays, gulfs, and other inlets are parts of these larger ocean systems.Major Divisions of the Ocean Floor
Continental Shelf
It is the extended margin of a continent, covered by shallow seas and gulfs.
Characteristics:
• Very gentle slope (average gradient of about 1° or less).
• Ends at a steep drop called the shelf break.
• Width varies: typically about 80 km wide but can be very narrow (e.g., near Chile or Sumatra) or extremely wide (e.g., the Siberian shelf, up to 1,500 km).
• Depth ranges from around 30 m to 600 m.
• Covered with sediments deposited by rivers, glaciers, and wind; over time, these sediments can form fossil fuels.
Continental Slope
It connects the continental shelf with the deep ocean basins.
Characteristics:
• Begins at the shelf break where the seafloor drops sharply.
• Has a gradient of 2–5°.
• Depth ranges from about 200 m to 3,000 m.
• Marks the end of the continental landmass and often features canyons and trenches.
Deep Sea Plain
These are vast, gently sloping, and very flat areas of the ocean floor.
Characteristics:
• Among the flattest and smoothest regions on Earth.
• Depths vary between 3,000 m and 6,000 m.
• Covered with fine-grained sediments like clay and silt.
Oceanic Deeps (Trenches)
These are the deepest, narrow, and steep-sided parts of the oceans.
Characteristics:
• Typically 3–5 km deeper than the surrounding seafloor.
• Occur along the bases of continental slopes and near island arcs.
• Associated with active volcanoes and earthquakes, making them important for studying plate tectonics.
• About 57 deeps have been explored: 32 in the Pacific, 19 in the Atlantic, and 6 in the Indian Ocean.
Minor Relief Features on the Ocean Floor
• Mid-Oceanic Ridges:
– Underwater mountain chains made of two parallel ranges separated by a central depression.
– Peaks can be as high as 2,500 m and sometimes emerge above sea level (e.g., Iceland on the mid-Atlantic Ridge).
• Seamounts:
– Underwater mountains with pointed summits that do not reach the surface.
– They are volcanic in origin and can be 3,000–4,500 m tall (e.g., the Emperor Seamount near the Hawaiian Islands).
• Submarine Canyons:
– Deep valleys, sometimes as vast as the Grand Canyon, cutting through continental shelves and slopes.
– Often start at the mouths of large rivers (e.g., Hudson Canyon).
• Guyots:
– Flat-topped seamounts that have subsided gradually over time.
– More than 10,000 seamounts and guyots are estimated in the Pacific Ocean alone.
• Atolls:
– Low islands in tropical oceans formed by coral reefs surrounding a central depression or lagoon, which can contain fresh, brackish, or saline water.
III. Temperature of Ocean Waters
How Ocean Temperature Works
• Ocean waters are heated by the sun, but heating and cooling occur more slowly than on land.
• The highest temperatures are always at the surface due to direct sunlight, with heat then moving downward by convection.Factors Influencing Temperature Distribution
Latitude:
Surface water temperature is highest at the equator and decreases toward the poles because of reduced solar energy.
Unequal Distribution of Land and Water:
Oceans in the northern hemisphere tend to be warmer because they are adjacent to larger landmasses.
Prevailing Winds:
Winds blowing from land toward the ocean can push warm surface water away from the coast, causing upwelling of cold water.
Conversely, onshore winds can cause warm water to pile up near the coast.
Ocean Currents:
Warm currents (e.g., the Gulf Stream) can raise temperatures in otherwise cold areas.
Cold currents (e.g., the Labrador Current) lower temperatures in warmer regions.
Temperature Distribution in the Ocean
• Horizontal Distribution:
– Enclosed seas in low latitudes are usually warmer than open seas; in high latitudes, enclosed seas are cooler.
• Vertical Distribution:
– The temperature decreases with increasing depth.
– A distinct layer called the thermocline begins about 100–400 m below the surface, where temperature drops rapidly.
– About 90% of the ocean’s water lies below the thermocline, where temperatures approach 0°C. • Layered Structure in Middle and Low Latitudes:
– First Layer (Surface Layer):
• About 500 m thick with temperatures between 20°C and 25°C.
• Present all year in tropical regions; seasonal in mid latitudes.
– Second Layer (Thermocline):
• Lies below the surface layer with a rapid decrease in temperature.
• Thickness of about 500–1,000 m.
– Third Layer (Deep Layer):
• Extremely cold, extending to the ocean floor. • In Polar Regions:
– Surface water temperatures are close to 0°C, resulting in only one layer of cold water throughout.Average Temperature Patterns
• Average surface temperature is about 27°C at the equator, decreasing roughly 0.5°C for every degree of latitude.
• Typical averages:
– Around 22°C at 20° latitude
– Around 14°C at 40° latitude
– Near 0°C close to the poles
• Northern hemisphere oceans generally record higher temperatures than southern hemisphere oceans.
• The highest ocean temperatures are found slightly north of the equator.
IV. Salinity of Ocean Waters
Understanding Salinity
• Salinity measures the amount of dissolved salt in seawater, usually expressed as parts per thousand (o/oo or ppt).
• It is calculated by the amount (in grams) of salt in 1,000 grams (1 kg) of seawater.
• A salinity of 24.7 o/oo is used as the upper limit to define “brackish water.”Factors Affecting Salinity
Evaporation and Precipitation:
Evaporation increases salinity by removing water, while precipitation decreases salinity by adding freshwater.
Freshwater Input:
River water and runoff lower salinity in coastal areas; in polar regions, the processes of freezing and thawing also affect it.
Wind:
Winds can transfer water from one area to another, influencing local salinity levels.
Ocean Currents:
Currents mix water masses, creating variations in salinity. • Salinity is closely related to temperature and density—changes in one often affect the others.
Regional Variations in Salinity
Open Ocean Salinity:
• Normal open ocean water has a salinity between 33 and 37 parts per thousand (o/oo).Special Regions:
• Red Sea: Being landlocked, it can reach up to 41 o/oo.
• Estuaries and the Arctic: Salinity fluctuates seasonally between 0 and 35 o/oo.
• Hot, Dry Regions: High evaporation can push salinity as high as 70 o/oo.Pacific Ocean:
• Its salinity varies mainly because of its shape and large area.
• On the western parts of the northern hemisphere, salinity decreases from about 35 o/oo to 31 o/oo due to melted water from the Arctic.
• South of 15°–20° latitude, salinity decreases further to around 33 o/oo.Atlantic Ocean:
• The average salinity is about 36 o/oo.
• The highest salinity is recorded between latitudes 15° and 20°.
• Maximum salinity (37 o/oo) is found between 20° N and 30° N and from 20° W to 60° W, then it gradually decreases towards the north.Other Regional Variations:
• North Sea: Even at higher latitudes, it has higher salinity because of saline water brought by the North Atlantic Drift.
• Baltic Sea: Shows low salinity due to a large amount of river water entering the sea.
• Mediterranean Sea: Has higher salinity due to intense evaporation.
• Black Sea: Records very low salinity because of the huge influx of freshwater from rivers.Indian Ocean:
• The average salinity is around 35 o/oo.
• Bay of Bengal: Has a low salinity trend due to significant river water input.
• Arabian Sea: Shows higher salinity because of high evaporation and a low influx of freshwater.
- Vertical Distribution of Salinity
• At the surface, salinity can increase when water is lost to evaporation or ice formation, or decrease when fresh water is added.
• Below the surface, salinity remains nearly constant because there is little loss or addition of water or salt.
• There is a noticeable difference between the lower-salinity surface water and the higher-salinity deep water, leading to a layer called the halocline where salinity rises sharply.
• The increase in salinity also increases water density, causing denser, saltier water to sink below less dense water, which leads to vertical stratification.