The NPSG is the largest of the gyres as well as the largest ecosystem on our planet. Like other subtropical gyres, it has a high-pressure zone in its center. Circulation around the center is clockwise around this high-pressure zone. Subtropical gyres make up 40% of the Earth’s surface and play critical roles in carbon fixation and nutrient cycling.[1] This particular gyre covers most of the Pacific Ocean and comprises four prevailing ocean currents: the North Pacific Current to the north, the California Current to the east, the North Equatorial Current to the south, and the Kuroshio Current to the west. Its large size and distance from shore has caused the NPSG to be poorly sampled and thus poorly understood.[2]
The main ocean currents involved with the North Pacific Gyre
The life processes in open-ocean ecosystems are a sink for the atmosphere’s increasing CO2. Gyres make up a large proportion, approximately 75%, of what we refer to as the open ocean, or the area of the ocean that does not consist of coastal areas. They are considered oligotrophic, or nutrient poor because they are far from terrestrial runoff.[3] These regions were once thought to be homogenous and static habitats. However, there is increasing evidence that the NPSG exhibits substantial physical, chemical, and biological variability on a variety of time scales.[2] Specifically, the NPSG exhibits seasonal and interannual variations in primary productivity (simply defined as the production of new plant material), which is important for the uptake of CO2.
The NPSG is not only a sink for CO2 in the atmosphere, but also other pollutants. As a direct result of this circular pattern, gyres act like giant whirlpools and become traps for anthropogenic pollutants, such as marine debris. The NPSG has become recognized for the large quantity of plastic debris floating just below the surface in the center of the gyre. This area has recently received a lot of media attention and is commonly referred to as the Great Pacific Garbage Patch.
History of discovery
The NPSG is not often sampled because of its distance from the coast and its shortage of marine life. These vast and deep ocean waters, far from the influence of land, have historically been considered the oceanic equivalent of terrestrial deserts, with low standing stocks of biomass and low production rates. This perspective is derived from a dearth of comprehensive investigation of central gyre habitats. Over the past two decades these views have been challenged with a newfound understanding of the dynamics of the NPSG.[4]
HMSChallenger embarked upon the first global marine research expedition in the 19th century.
During the early days of marine exploration, HMSChallenger (1872–1876), on its leg from Yokohama to Honolulu, collected plant and animal specimens as well as numerous seawater samples.[2] The goals of this expedition were to determine the chemical composition of seawater and the organic matter in suspension and to study the distribution and abundance of various communities of organisms. The motivation for studying open ocean ecosystems has changed over time, whereas today more modern studies focus on biodiversity and the effects of climate on ecosystem dynamics. Today, the Hawaii Ocean Time-series (HOT) program has assembled the largest and most comprehensive ecological data set for the NPSG and is scheduled to continue to the next millennium.[2] Programs like HOT have debunked the hypothesis that this ecosystem is static and homogenous, finding that the NPSG exhibits dynamic seasonal patterns separating it from other open ocean systems.
Physical characteristics
The NPSG is the largest of the open ocean habitats and is considered to be the Earth’s largest contiguous biome.[5] This great anticyclonic circulation feature extends from 15°N to 35°N latitude and from 135°E to 135°W longitude. Its surface area spans approximately 2 x 107km2. Its western portion, west of 180° longitude, has greater physical variability than the eastern portion. This variability, where different weather patterns affect subregions differently, is due to the large dimensions of this gyre.[2]
This large variability is caused by discrete eddies, near-inertial motions, and internal tides.[2] Climate patterns such as the North Pacific Gyre Oscillation (NPGO), El Nino/Southern Oscillation (ENSO) and the Pacific Decadal Oscillation (PDO) affect the interannual variability in primary productivity in the NPSG.[3] DiLorenzo et al., 2008 These conditions can have profound effects on biological processes within this habitat,[2] they have the ability to shift sea surface temperature (SST), chlorophyll patterns, nutrient patterns, oxygen concentrations, mixed layer depths, and thus the carrying capacity (amount of life this habitat can carry) of the NPSG.
Nutrient cycling
Low nutrient concentrations and thus a low density of living organisms characterize the surface waters of the NPSG. The low biomass results in clear water, allowing photosynthesis to occur to a substantial depth. The NPSG is classically described as a two-layered system. The upper, nutrient-limited layer accounts for most of the primary production, supported primarily by recycled nutrients. The lower layer has nutrients more readily available, but photosynthesis is light-limited.[4]
In open-ocean systems, biological production depends on intense nutrient recycling within the euphotic (sunlit) zone, with only a small fraction supported by the input of “new” nutrients.[6] Previously there was a perception that the NPSG was a marine desert and that “new” nutrients were not commonly added to this system. The outlook has changed, as scientists have begun to have a better understanding of this habitat.[2] Although fairly high rates of primary production are maintained through rapid recycling of nutrients,[4] physical processes such as internal waves and tides, cyclonic mesoscale eddies, wind-driven Ekman pumping, and atmospheric storms may carry in new nutrients.[7]
Nutrients that do not get used up on the surface will eventually sink down and nourish the seafloor habitat. The deep benthic habitats of the ocean gyres have been thought to typically consist of some of the most food-poor regions on the planet.[8] One of the sources of nutrients to this deep ocean habitat is marine snow. Marine snow consists of detritus, dead organic matter, which falls from the surface waters where productivity is highest and exports carbon and nitrogen from the surface mixed layer to the deep ocean. Data on the abundance of marine snow to the deep ocean floor is lacking in this large ecosystem.[9] However, Pilskaln et al. found that in the NPSG, marine snow was at a higher abundance than expected and were surprisingly comparable to a deep coastal upwelling system.
Higher nutrient value may be because of Rhizosolenia mats, which also play an important role in contributing to marine snow in subtropical gyres. These are generally multi-species associations of Rhizosolenia species of diatoms. This larger phytoplankton may reach up to tens of centimeters in size.[9] These mats are particularly abundant in the NPSG. Their abundance in this ecosystem suggests a higher flux of nutrients in the NPSG than was predicted in classic theories.
Zooplankton can migrate nutrients across different vertical levels of ocean.
While N is transported deeper by this mechanism, the surface waters are potentially cut off from this source. Nitrogen must be available for life at the surface. In order to account for this lack of nitrogen to the surface, there are organisms that are capable of nitrogen fixation in the NPSG. Trichodesmium is one species capable of nitrogen fixation that is found in many surface plankton blooms.[7] Nitrogen fixation is the process where inert N2 is taken from the atmosphere and converted into a nitrogen compound that is available to organisms for use. In many oligotrophic marine ecosystems, nitrogen fixation is a common source of nitrogen.
Vertically migrating zooplankton can also actively transport nutrients to different zones of the water column. Zooplankton feed in the surface waters at night, and then by day release fecal pellets to the midwaters, which can transport C, N, and P to the deeper waters. In the NPSG the zooplankton community is not static but fluctuates seasonally and is dominated by copepods, euphausiids, and chaetognaths.[6]
Recently, classic theories about the lack of nutrients in the NPSG have been disproven and new theories suggest that the ecosystem actually is dynamic and characterized by strong seasonal, interannual, and even decadal variability[9] It has also been deemed highly sensitive to climate change, scientists have observed increases in water column stratification and decreased inorganic nutrient availability. These changes are proposed as driving mechanisms that are changing the current trend in phytoplankton community structure from eukaryotic to prokaryotic populations, as these simpler organisms can withstand lower nutrient supply.[9] Zooplankton and phytoplankton represent less than 10% of living organisms in this region, and it is now well documented that the NPSG is a “microbial ecosystem”.[2]
Microbial community
Microbial organisms make up the majority of the primary producers in the NPSG. They are autotrophic, meaning they capture their own “food” from sunlight and chemicals, including CO2. These organisms comprise the base of the food chain, and thus their presence in an ecosystem is fundamental. In the NPSG, primary productivity is often described as low.
Before 1978, scientists hypothesized that diatoms dominated plankton populations in the NPSG. The primary consumers were expected to be relatively large mesozooplankton.[2] It is now well known that most of the algae in the NPSG are actually bacteria (unicellular organisms), dominated by cyanobacteria, or blue-green algae. These simple organisms make up the majority of the standing stock of photosynthesizing marine life in this ecosystem. Scientists have also recently discovered Archaea (also a single-celled microorganism, but more similar to a eukaryote than bacteria) genes in the NPSG, suggesting that additional diversity exists in this habitat. Many microorganisms may exist in this gyre because small body size has a competitive advantage in the ocean for resource (light and nutrients) acquisition.[2] In the contemporary view of the NPSG, the microbial food web is always present, whereas the larger eukaryote-grazer food chain is seasonal and ephemeral.[2]
Eukaryotic plankton community
Phytoplankton are a form of Eukaryotic plankton found in oceans.
Eukaryotic plankton in the gyre is dependent on “new” nutrients coming in from physical weather patterns. The classic two-layered model discussed in previous sections considers the upper layer to be equivalent to a “spinning wheel,” with little export of nutrients because they are constantly recycled. This model does not allow for the input of new nutrients, which is problematic because this would make any rapid increase, or bloom of phytoplankton impossible. Despite ever-present nutrient limitation in the upper portion, plankton biomass and rates of primary production have considerable temporal variability and do produce blooms in the NPSG.[3]
This interannual variability has been attributed to alterations in upper ocean nutrient supply stemming from physical variations due to ENSO and PDO.[3] Based on new data, it now appears that present rates of primary production in these low nutrient regions are much greater than had been considered, and can vary significantly on time scales ranging from daily to interdecadal.[2] In the spring, rapid increases in surface phytoplankton are occasionally observed in association with cyclonic mesoscale eddies or intense atmospheric disturbances, both physical processes that bring in new nutrients.[4] In the summer, blooms are seen more regularly and are typically dominated by diatoms and cyanobacteria. These regular summer blooms may be caused by variations in the PDO.[3] Summer blooms have been observed in these waters as long as research vessels have been frequenting them. All of these blooms have been seen in the eastern part of the NSPG with none reported west of 160° W.[4] Hypotheses to explain this phenomenon are that the gyre is characterized by low phosphate, but that the bloom region of the eastern NPSG has considerably higher phosphate concentrations than the western.[4]
Variations in primary production in the NPSG can significantly affect nutrient cycling, food-web dynamics, and global elemental fluxes.[3] The size distribution of pelagic primary producers determines both the composition and magnitude of the exported nutrients to the deeper waters.[2] This in turn affects the communities that live in the deeper waters of this system.
Mesopelagic community
The mesopelagic zone is sometimes referred to as the twilight zone; it extends from 200m to around 1000m. In the deeper layers of the NPSG, species higher up on the food chain will migrate vertically or horizontally within or in and out of the gyre. Based on analyses of the zooplankton community, the Central North Pacific has a high species diversity (or high number of species) and high equitability (meaning relatively equal numbers of each exist). There is also a low degree of seasonal variability of densities of zooplankton.[2]
Studies of mesopelagic fishes of central subtropical waters are scarce. The few studies that do exist found that mesopelagic fish species are not uniformly distributed throughout the subtropical Pacific Ocean. Their geographic ranges conform to patterns shown by zooplankton. Some of the species found are restricted to these low-productivity central gyres. Some of the families of fish that are highly represented are Mytophids, Gonostomatids, Photichthyids, Sternoptychids, and Melamphaids.[10] Our understanding of the mesopelagic community of the NPSG suffers from an insufficiency of data due to the difficulty of accessing the deeper zones of this system.
Benthic community
The deepest community in the NPSG is the benthic community. At the depths of the gyre lies a sea floor of fine-grained clay sediments. This sediment is home to a community of organisms, which generally receive their nutrients as a “rain” of productivity sinking from above. At depth under the gyre lies one of the most food-poor areas on the planet, which therefore supports very low densities and biomass of benthic infauna, or animals residing in the sediment.[8] In the sediment itself, nutrients generally decline with depth, including carbon, chlorophyll, and nitrogen. Density of the benthic infauna is consistent with this nutrient pattern. Infauna are typically found in the shallower layers of sediments where the sediment-water interface lies and generally decrease in number with increasing depth in the sediment.[11] Bacteria in the sediment show this pattern as well as macrofauna (infaunal organisms >0.5mm), which are dominated by agglutinating (soft-bodied) foraminifera and nematodes. Other prominent macrofauna found in the sediment are calcareous foraminifera, copepods, polychaetes, and bivalves.[11] These benthic organisms rely heavily on the supply of nutrients that settle to the sea floor. Any change in primary production at the surface could pose a major threat to these organisms, as well as cause other potential negative outcomes to other parts of the NPSG.
Future and importance of the NPSG
Plastic garbage washed ashore from the Pacific Ocean
Until recently the NPSG was considered to be a static part of a vast global marine desert. Recent discoveries have proved that this system is dynamic and contains physical, chemical, and biological variability on a variety of time scales. With the current changing climate, patterns in the atmosphere are shifting and causing changes in primary production in the NPSG. Variations in primary productivity can affect the ocean carbon cycle and potentially atmospheric CO2 and climate, because such variations can change the amount of carbon that is stored in the subsurface layers of the oceans.[12] Because the NPSG is the largest contiguous biome on earth, it is not only important to a community of organisms, but also the rest of the planet.
The NPSG has received copious attention because of another issue it currently faces. The eddy effects of the gyre serve to retain pollutants in its center. If a pollutant gets trapped in a current that is headed toward a gyre, it will stay there indefinitely or as long as the life of the pollutant. One such pollutant that is persistent and common in the NPSG is plastic debris. The NPSG forces debris into its central area. This phenomenon has recently given this gyre the nickname, “The Pacific Garbage Patch.” The mean abundance and weight of plastic pieces in this area are currently the largest observed in the Pacific Ocean.[13] It is rumored that this plastic “soup” is anywhere from the size of Texas to the size of the US. With increasing interest in pollution and climate change, the NPSG has gained more attention. It is important that our knowledge of this system continue to flourish for these reasons, as well as solely for the understanding of the world’s largest ecosystem.
Plankton are the diverse collection of organisms found in water that are unable to propel themselves against a current. The individual organisms constituting plankton are called plankters. In the ocean, they provide a crucial source of food to many small and large aquatic organisms, such as bivalves, fish and whales.
Zooplankton are the animal component of the planktonic community. Plankton are aquatic organisms that are unable to swim effectively against currents. Consequently, they drift or are carried along by currents in the ocean, or by currents in seas, lakes or rivers.
Upwelling is an oceanographic phenomenon that involves wind-driven motion of dense, cooler, and usually nutrient-rich water from deep water towards the ocean surface. It replaces the warmer and usually nutrient-depleted surface water. The nutrient-rich upwelled water stimulates the growth and reproduction of primary producers such as phytoplankton. The biomass of phytoplankton and the presence of cool water in those regions allow upwelling zones to be identified by cool sea surface temperatures (SST) and high concentrations of chlorophyll-a.
The biological pump (or ocean carbon biological pump or marine biological carbon pump) is the ocean's biologically driven sequestration of carbon from the atmosphere and land runoff to the ocean interior and seafloor sediments. In other words, it is a biologically mediated process which results in the sequestering of carbon in the deep ocean away from the atmosphere and the land. The biological pump is the biological component of the "marine carbon pump" which contains both a physical and biological component. It is the part of the broader oceanic carbon cycle responsible for the cycling of organic matter formed mainly by phytoplankton during photosynthesis (soft-tissue pump), as well as the cycling of calcium carbonate (CaCO3) formed into shells by certain organisms such as plankton and mollusks (carbonate pump).
The mesopelagiczone, also known as the middle pelagic or twilight zone, is the part of the pelagic zone that lies between the photic epipelagic and the aphotic bathypelagic zones. It is defined by light, and begins at the depth where only 1% of incident light reaches and ends where there is no light; the depths of this zone are between approximately 200 to 1,000 meters below the ocean surface.
The Humboldt Current, also called the Peru Current, is a cold, low-salinity ocean current that flows north along the western coast of South America. It is an eastern boundary current flowing in the direction of the equator, and extends 500–1,000 km (310–620 mi) offshore. The Humboldt Current is named after the German naturalist Alexander von Humboldt even though it was discovered by José de Acosta 250 years before Humboldt. In 1846, von Humboldt reported measurements of the cold-water current in his book Cosmos.
The Kuroshio Current, also known as the Black or Japan Current or the Black Stream, is a north-flowing, warm ocean current on the west side of the North Pacific Ocean basin. It was named for the deep blue appearance of its waters. Similar to the Gulf Stream in the North Atlantic, the Kuroshio is a powerful western boundary current that transports warm equatorial water poleward and forms the western limb of the North Pacific Subtropical Gyre. Off the East Coast of Japan, it merges with the Oyashio Current to form the North Pacific Current.
The Canary Current is a wind-driven surface current that is part of the North Atlantic Gyre. This eastern boundary current branches south from the North Atlantic Current and flows southwest about as far as Senegal where it turns west and later joins the Atlantic North Equatorial Current. The current is named after the Canary Islands. The archipelago partially blocks the flow of the Canary Current.
The spring bloom is a strong increase in phytoplankton abundance that typically occurs in the early spring and lasts until late spring or early summer. This seasonal event is characteristic of temperate North Atlantic, sub-polar, and coastal waters. Phytoplankton blooms occur when growth exceeds losses, however there is no universally accepted definition of the magnitude of change or the threshold of abundance that constitutes a bloom. The magnitude, spatial extent and duration of a bloom depends on a variety of abiotic and biotic factors. Abiotic factors include light availability, nutrients, temperature, and physical processes that influence light availability, and biotic factors include grazing, viral lysis, and phytoplankton physiology. The factors that lead to bloom initiation are still actively debated.
High-nutrient, low-chlorophyll (HNLC) regions are regions of the ocean where the abundance of phytoplankton is low and fairly constant despite the availability of macronutrients. Phytoplankton rely on a suite of nutrients for cellular function. Macronutrients are generally available in higher quantities in surface ocean waters, and are the typical components of common garden fertilizers. Micronutrients are generally available in lower quantities and include trace metals. Macronutrients are typically available in millimolar concentrations, while micronutrients are generally available in micro- to nanomolar concentrations. In general, nitrogen tends to be a limiting ocean nutrient, but in HNLC regions it is never significantly depleted. Instead, these regions tend to be limited by low concentrations of metabolizable iron. Iron is a critical phytoplankton micronutrient necessary for enzyme catalysis and electron transport.
In oceanic biogeochemistry, the f-ratio is the fraction of total primary production fuelled by nitrate. The ratio was originally defined by Richard Eppley and Bruce Peterson in one of the first papers estimating global oceanic production. This fraction was originally believed significant because it appeared to directly relate to the sinking (export) flux of organic marine snow from the surface ocean by the biological pump. However, this interpretation relied on the assumption of a strong depth-partitioning of a parallel process, nitrification, that more recent measurements has questioned.
A lake ecosystem or lacustrine ecosystem includes biotic (living) plants, animals and micro-organisms, as well as abiotic (non-living) physical and chemical interactions. Lake ecosystems are a prime example of lentic ecosystems, which include ponds, lakes and wetlands, and much of this article applies to lentic ecosystems in general. Lentic ecosystems can be compared with lotic ecosystems, which involve flowing terrestrial waters such as rivers and streams. Together, these two ecosystems are examples of freshwater ecosystems.
Marine habitats are habitats that support marine life. Marine life depends in some way on the saltwater that is in the sea. A habitat is an ecological or environmental area inhabited by one or more living species. The marine environment supports many kinds of these habitats. Marine habitats can be divided into coastal and open ocean habitats. Coastal habitats are found in the area that extends from as far as the tide comes in on the shoreline out to the edge of the continental shelf. Most marine life is found in coastal habitats, even though the shelf area occupies only seven percent of the total ocean area. Open ocean habitats are found in the deep ocean beyond the edge of the continental shelf.
A planktivore is an aquatic organism that feeds on planktonic food, including zooplankton and phytoplankton. Planktivorous organisms encompass a range of some of the planet's smallest to largest multicellular animals in both the present day and in the past billion years; basking sharks and copepods are just two examples of giant and microscopic organisms that feed upon plankton. Planktivory can be an important mechanism of top-down control that contributes to trophic cascades in aquatic and marine systems. There is a tremendous diversity of feeding strategies and behaviors that planktivores utilize to capture prey. Some planktivores utilize tides and currents to migrate between estuaries and coastal waters; other aquatic planktivores reside in lakes or reservoirs where diverse assemblages of plankton are present, or migrate vertically in the water column searching for prey. Planktivore populations can impact the abundance and community composition of planktonic species through their predation pressure, and planktivore migrations facilitate nutrient transport between benthic and pelagic habitats.
Haida Eddies are episodic, clockwise rotating ocean eddies that form during the winter off the west coast of British Columbia’s Haida Gwaii and Alaska’s Alexander Archipelago. These eddies are notable for their large size, persistence, and frequent recurrence. Rivers flowing off the North American continent supply the continental shelf in the Hecate Strait with warmer, fresher, and nutrient-enriched water. Haida eddies are formed every winter when this rapid outflow of water through the strait wraps around Cape St. James at the southern tip of Haida Gwaii, and meets with the cooler waters of the Alaska Current. This forms a series of plumes which can merge into large eddies that are shed into the northeast Pacific Ocean by late winter, and may persist for up to two years.
The lipid pump sequesters carbon from the ocean's surface to deeper waters via lipids associated with overwintering vertically migratory zooplankton. Lipids are a class of hydrocarbon rich, nitrogen and phosphorus deficient compounds essential for cellular structures. This lipid carbon enters the deep ocean as carbon dioxide produced by respiration of lipid reserves and as organic matter from the mortality of zooplankton.
The viral shunt is a mechanism that prevents marine microbial particulate organic matter (POM) from migrating up trophic levels by recycling them into dissolved organic matter (DOM), which can be readily taken up by microorganisms. The DOM recycled by the viral shunt pathway is comparable to the amount generated by the other main sources of marine DOM.
Benthic-pelagic coupling are processes that connect the benthic zone and the pelagic zone through the exchange of energy, mass, or nutrients. These processes play a prominent role in both freshwater and marine ecosystems and are influenced by a number of chemical, biological, and physical forces that are crucial to functions from nutrient cycling to energy transfer in food webs.
Low-nutrient, low-chlorophyll (LNLC)regions are aquatic zones that are low in nutrients and consequently have low rate of primary production, as indicated by low chlorophyll concentrations. These regions can be described as oligotrophic, and about 75% of the world's oceans encompass LNLC regions. A majority of LNLC regions are associated with subtropical gyres but are also present in areas of the Mediterranean Sea, and some inland lakes. Physical processes limit nutrient availability in LNLC regions, which favors nutrient recycling in the photic zone and selects for smaller phytoplankton species. LNLC regions are generally not found near coasts, owing to the fact that coastal areas receive more nutrients from terrestrial sources and upwelling. In marine systems, seasonal and decadal variability of primary productivity in LNLC regions is driven in part by large-scale climatic regimes leading to important effects on the global carbon cycle and the oceanic carbon cycle.
Eddy pumping is a component of mesoscale eddy-induced vertical motion. It is a physical mechanism through which vertical motion is created from variations in an eddy's rotational strength. Cyclonic (Anticyclonic) eddies lead primarily to upwelling (downwelling) in the Northern Hemisphere and vice versa in the Southern hemisphere. It is a key mechanism driving biological and biogeochemical processes in the ocean such as algal blooms and the carbon cycle.
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