Marine Ecology Flashcards
(137 cards)
Describe and explain the seasonal cycle of biological activity (e.g., phytoplankton, zooplankton and fish biomass and production) in the pelagic.
Other factors influence phytoplankton growth rates, including water temperature and salinity, water depth, wind, and what kinds of predators are grazing on them. Phytoplankton can grow explosively over a few days or weeks. Basically, the seasonal cycle is driven by sea-surface temperature and the onset of the thermocline leading to phytoplankton blooms during spring, the prevalence of thermal stratification leading to exhaustion of nutrients and subsequent demise of phytoplankton during summer-autumn, and remixing and regeneration of nutrients during winter.
Plankton predominantly comprises short-lived organisms. As a rule, these reproduce so rapidly that several generations may be produced within a single year. The development of planktonic organisms generally follows a regular annual cycle that begins with a spring bloom of the phytoplankton.
Fish biomass:
LOOK AT SLIDES
Explain how environmental factors and the species diversity and biomass of benthic communities vary from the continental shelf to the deep sea.
There are a lot of factors that can affect benthic biodiversity along a depth gradient like water temperature, light availability, oxygen (and other elements) concentration and pressure.
Interactions between pelagic and benthic environments are related to a variety of abiotic and biotic processes that have a major influence on the structure and dynamics of marine ecosystems. Transport of particulate and dissolved materials, gases, as well as living organisms, and also sedimentation and erosion are subsumed under these processes that induce a shifting of materials between benthic and pelagic material pools and vice versa. Imbalances in these transactions result in a change of biotic structures and have far-reaching consequences for the development of the communities. Exchange processes are either directed from water to the bottom sediment (termed as pelagic–benthic) or reversed (termed as benthic–pelagic), and impact on abiotic material pools as well as on the biota, such as producers and consumers, or can be related to the exchange between abiotic and biotic material components.
Describe and explain intertidal zonation on rocky shores
Intertidal zonation refers to the frequently observed pattern by which species replace one another along a gradient from the low to high tide lines along many of the world’s coastlines.
variation in the distribution of organisms caused by differences in both biotic and abiotic conditions along an environmental gradient. Organisms living on the rocky shore have different adaptations to these factors and therefore will be able to survive at different heights on the shore accordingly.
The intertidal zone or littoral zone is the shoreward fringe of the seabed between the highest and lowest limit of the tides. The upper limit is often controlled by physiological limits on species tolerance of temperature and drying. The lower limit is often determined by the presence of predators or competing species.
The rocky intertidal ecosystem can be divided into four zones: the splash zone, high intertidal, middle intertidal, and low intertidal
What is the Coriolis effect (force)?
Apparent deflection of a moving object when viewed from a rotating frame of reference.
Freely moving objects on the surface of the Earth experience the ‘Coriolis force’.
On a non-rotating planet, ocean currents (and winds) would flow directly from areas of high pressure to low pressure.
Because Earth rotates, currents (and winds) flow to the right of this direction north of the equator, and to the left of this direction south of the equator.
What is Ekman Transport?
Friction between wind and water surface causes water to move in direction of wind.
The Coriolis effect deflects this current.
The surface layer drags the layer beneath, which is also deflected.
The net movement of the ocean’s surface layer is perpendicular to the right of the wind in the Northern Hemisphere and to the left in the Southern Hemisphere.
Deep Ocean Circulation and Thermohaline Circulation
Thermohaline circulation is due to differences in the density that arise from variations of temperature and salinity.
thermo = heat
haline = salt (halide ions)
Solar radiation warms waters in the tropics, causing them to expand (become less dense) and float.
The ocean loses heat to the atmosphere at high latitudes (air colder than water), causing the surface waters to cool and contract (become denser) and sink.
What affects the density of sea water?
Density = mass/volume
Units kg m-3
Density increases as temperature decreases
Density increases as salinity increases
Density increases during ice formation because salt is excluded from the ice
Density decreases following rain due to dilution of salt
Mechanisms of Deep Water Formation
The mechanisms of deep-water formation are different in North & South Atlantic.
In the North Atlantic, high salinity water (brought north by the Gulf Stream) is cooled in winter leading to deep convective mixing.
On the Antarctic continental shelf, ice formation increases salinity and upon further cooling, the dense water flows off the shelf and down the continental slope.
Thermohaline Conveyor Belt
North Atlantic Deep Water flows south along the western side of the N. Atlantic.
Antarctic Bottom Water is the densest water and flows north along the western side of the S Atlantic.
These two deep currents meet in the S. Atlantic and flow eastward into the Indian and S. Pacific Oceans
The deep water flows from the Atlantic to the Pacific, are balanced by a return flow of warm surface waters from the Pacific to the Indian and back to the Atlantic Ocean.
The combination of these slow deep and surface water flows is referred to as a conveyor belt.
The thermohaline circulation is sluggish compared with the wind-driven circulation.
The entire circulation and replacement of the deep waters takes about 1000 years
750 years for the Atlantic
1500 years for the Pacific
What is an ion?
an ion is a charged atom or charged molecule
ions form by adding or removing one or more electrons from an atom or molecule
a cation is a positively charged ion
e.g., sodium ion: Na+
an anion is a negatively charged ion
e.g., chloride: Cl-
sulfate: SO42-
ionic bonds hold crystals together
e.g., sodium chloride (= table salt): NaCl
Why is water sometimes described as a universal solvent?
Water (H2O) can dissolve more things than any other natural substance.
It is a polar molecule, that can form hydrogen bonds.
Water is good at dissolving salts
which consist of positively (+) and negatively (-) charged ions
NaCl → Na+ + Cl-
What are the sources of the ions in seawater?
Runoff from the continents (weathering of rocks) Na+ , K+, Ca2+ , Mg2+ Volcanic activity (hydrothermal vents) HS- , Cl-
How does the rule of constant proportions make measuring salinity easier?
The rule of constant proportions states that the relative amounts of the various ions in seawater are always the same (e.g., independent of salinity)
e.g.
Chloride = 55.03% of salinity everywhere in the sea
Sodium = 30.59% of salinity everywhere in the sea
the rule holds for other major ions
This allows chloride, which is easy to measure, to be used to calculate salinity
Chlorinity = mass of chloride in a kg of seawater
Conductivity is now commonly used to measure salinity in practical salinity units (psu)
1 psu = 1 ‰ or 1 ppt
Limiting Nutrients
The two main limiting nutrient elements for biological production in sea are nitrogen (N) and phosphorus (P).
These are present as dissolved inorganic ions
phosphate: PO43-
nitrate : NO3-
Concentrations of these ions are often very low in surface waters.
Productivity of the oceans often depends on the regeneration (recycling) of inorganic N and P from organic matter.
Vertical profiles of dissolved O2
Feature: oxygen minimum zone
located in thermocline
high respiration rate
limited exchange of water
What are Biogeochemical cycles?
Pathways by which a chemical element moves through different compartments (called reservoirs).
Examples Carbon cycle Nitrogen cycle Sulphur cycle Phosphorus cycle
The Carbon cycle
CO2 moves between ocean and atmosphere due to physical-chemical processes (Solubility pump).
C is exchanged between the ocean and the biota via:
Photosynthesis removes CO2 from the atmosphere and ocean.
CO2 + H2O + light → CH2O + O2
Respiration releases CO2 to the atmosphere and ocean:
CH2O + O2 → CO2 + H2O
Carbon enters the foodweb via grazing
Carbon is returned to the ocean as CO2 via respiration
Some primary produces will sink when they die, sequestering (storing) carbon in sediments
Dead stuff becomes detritus/POM (Particulate organic matter) which can be:
Decomposed by bacteria, producing CO2, POM, and DOM (Dissolved organic matter)
Feed on by animals, returning carbon to the foodweb
detritus/POM that is not decomposed sinks, sequestering carbon in sediments
The biological pump
Phytoplankton and macro-algae (seaweed) fix carbon
Incorporating C into the food chain (grazing) - or releasing it as DOC/POC
Feacal pellets, marine snow, and dead marine organisms sink to the deeper layers
Where they decay consuming dissolved oxygen and giving off CO2.
Upwelling returns this CO2 to the epipelagic.
The biological pump requires the input of nutrients (N, P) to sustain plankton blooms.
Microbes and the carbon cycle
Play a critical role in all nutrient cycles
Fixing carbon
Link to the food chain
Also a source of CO2
Microbial action can make carbon inaccessible recalcitrant – RDOM
This sinks and can be stored for 1000s of years
Microbes decompose POM and DOM, producing dissolved CO2
Microbes degrade the most assessable carbon first.
Carbon that is harder to degrade, called recalcitrant carbon (RDOM), sinks before is can be degraded and is stored in sediments.
The balance between how much carbon sinks and how much is releases is critical in global carbon budgets.
The Nitrogen cycle
Nitrogen is fixed by bacteria and cyanobacteria
Key players: Trichodesmium spp.
Atelocyanobacterium spp.
(cyanobacteria)
Bacteria and archaea cycle nitrogen between ammonia, nitrites, and nitrates via nitrification (aerobic)
Fixed nitrogen and nitrates are taken into the biota and cycle through the food web
This nitrogen can be excreted as DON, or sink when taxa die (POM).
Bacteria and archaea recycle POM and DON in decomposition (ammonification)
Nitrogen is returned to the atmosphere via bacterial Denitrification (anaerobic)
The phosphorus cycle
Not found as a gas (Contrast to Carbon and Nitrogen)
Normally as part of a phosphate ion: PO43-
Found as salts in ocean sediments or in rocks.
Uplift brings ocean sediments to land.
Phosphate becomes available by chemical weathering.
Input to oceans is via rivers.
Enters the foodweb through uptake by plants, algae and bacteria.
Dissolved phosphate is precipitated and sinks into sediments
More on Limiting nutrients
Nutrients, particularly N and P, limit the fertility of many undisturbed ecosystems.
P is typically the main limiting nutrient in freshwaters, followed by N.
N is usually most limiting in marine systems, followed by P.
Although CO2 may limit photosynthesis in terrestrial plants, inorganic C is rarely limiting in aquatic systems.
The micronutrient Fe, has recently been found to be the main limiting nutrient over about 1/3 of the ocean surface – Iron fertilisation hypothesis.
Jawless Fish (Agnatha)
cylindrical, elongated body cartilaginous skull lack vertebrae lack jaws lack scales feed by suction using a round muscular mouth and sharp teeth
Hagfishes
Marine Jawless elongate fish Lack fins No vertebra (sort of) Burrow in muddy bottoms at moderate depths in cold waters Feed mainly on dead or dying fish Produce slime!