{"id":221,"date":"2017-01-23T16:35:54","date_gmt":"2017-01-23T16:35:54","guid":{"rendered":"https:\/\/pressbooks.ccconline.org\/introduction-to-oceanography\/chapter\/6-3-density\/"},"modified":"2021-10-26T21:10:21","modified_gmt":"2021-10-26T21:10:21","slug":"6-3-density","status":"publish","type":"chapter","link":"https:\/\/pressbooks.ccconline.org\/introduction-to-oceanography\/chapter\/6-3-density\/","title":{"raw":"6.3 Density","rendered":"6.3 Density"},"content":{"raw":"Density refers to the amount of mass per unit volume, such as grams per cubic centimeter (g\/cm3<\/sup>). The density of fresh water is 1 g\/cm3<\/sup> at 4o<\/sup> C (see section 5.1<\/a>), but the addition of salts and other dissolved substances increases surface seawater density to between 1.02 and 1.03 g\/cm3<\/sup>. The density of seawater can be increased by reducing its temperature, increasing its [pb_glossary id=\"1096\"]salinity[\/pb_glossary], or increasing the pressure. Pressure has the least impact on density as water is fairly incompressible, so pressure effects are not very significant except at extreme depths. However, if not for the slight compression of water due to pressure, sea level would be approximately 50 m higher than it is today! That leaves temperature and salinity as the primary factors determining density, and of these, temperature has the greatest impact (Figure 6.3.1).\r\n\r\n \r\n\r\n[caption id=\"attachment_219\" align=\"aligncenter\" width=\"1024\"]\"Global<\/a> Figure 6.3.1<\/strong> Global sea surface density. Colder polar regions display higher densities than warmer tropical zones (By Plumbago (Own work) [CC BY-SA 3.0, or GFDL (http:\/\/www.gnu.org\/copyleft\/fdl.html)], via Wikimedia Commons).[\/caption]Since temperature has the greatest effect on density, density profiles are usually mirror images of temperature profiles (Figure 6.3.2). Density is lowest at the surface, where the water is the warmest. As depth increases, there is a region of rapidly increasing density with increasing depth, which is called the [pb_glossary id=\"1062\"]pycnocline[\/pb_glossary]<\/strong>. The pycnocline coincides with the [pb_glossary id=\"1222\"]thermocline[\/pb_glossary], as it is the sudden decrease in temperature that leads to the increase in density. Below the pycnocline, density may be fairly constant (as is temperature), or it may continue to increase slightly towards the bottom.\r\n\r\n[caption id=\"attachment_220\" align=\"aligncenter\" width=\"635\"]\"Representative<\/a> Figure 6.3.2<\/strong> Representative density profile for the open ocean at mid-latitudes. The warm surface water causes a decrease in surface density (PW).[\/caption]\r\n\r\nThe profile above represents a stable state, or a high degree of stratification, where the warm, low density layer sits atop the colder, denser layer. If denser water happened to form at the surface, the water masses would be unstable, and the denser water would sink to the bottom, to be replaced by less dense water at the surface. This vertical movement of water masses based on density (as determined by temperature and salinity) is referred to as [pb_glossary id=\"1224\"]thermohaline circulation[\/pb_glossary], which is the topic of section 9.8<\/a>.\u00a0 By creating a stratified water column, the [pb_glossary id=\"1222\"]thermocline [\/pb_glossary] and [pb_glossary id=\"1062\"]pycnocline [\/pb_glossary] together create a barrier that prevents mixing between the warmer, less dense surface water and the colder, denser bottom water. In this way, nutrient-rich deep water may be prevented from coming to the surface to support [pb_glossary id=\"1603\"]primary production[\/pb_glossary].\r\n\r\nAs with temperature, there are also latitudinal differences in density. In the tropics the surface water is warm and low density, and there is a pronounced thermocline separating it from the colder, denser deep water. As stated above, this stratification prevents nutrient-rich water from reaching the surface and as a result tropical regions often have low productivity. In the high latitudes the water is uniformly cold at all depths, so there is little density stratification. The lack of a pycnocline (or a thermocline) allows cold, nutrient-rich deep water to more easily mix with the surface water, leading to higher primary production in polar regions.","rendered":"

Density refers to the amount of mass per unit volume, such as grams per cubic centimeter (g\/cm3<\/sup>). The density of fresh water is 1 g\/cm3<\/sup> at 4o<\/sup> C (see section 5.1<\/a>), but the addition of salts and other dissolved substances increases surface seawater density to between 1.02 and 1.03 g\/cm3<\/sup>. The density of seawater can be increased by reducing its temperature, increasing its salinity<\/a>, or increasing the pressure. Pressure has the least impact on density as water is fairly incompressible, so pressure effects are not very significant except at extreme depths. However, if not for the slight compression of water due to pressure, sea level would be approximately 50 m higher than it is today! That leaves temperature and salinity as the primary factors determining density, and of these, temperature has the greatest impact (Figure 6.3.1).<\/p>\n

 <\/p>\n

\"Global<\/a>
Figure 6.3.1<\/strong> Global sea surface density. Colder polar regions display higher densities than warmer tropical zones (By Plumbago (Own work) [CC BY-SA 3.0, or GFDL (http:\/\/www.gnu.org\/copyleft\/fdl.html)], via Wikimedia Commons).<\/figcaption><\/figure>\n

Since temperature has the greatest effect on density, density profiles are usually mirror images of temperature profiles (Figure 6.3.2). Density is lowest at the surface, where the water is the warmest. As depth increases, there is a region of rapidly increasing density with increasing depth, which is called the pycnocline<\/a><\/strong>. The pycnocline coincides with the thermocline<\/a>, as it is the sudden decrease in temperature that leads to the increase in density. Below the pycnocline, density may be fairly constant (as is temperature), or it may continue to increase slightly towards the bottom.<\/p>\n

\"Representative<\/a>
Figure 6.3.2<\/strong> Representative density profile for the open ocean at mid-latitudes. The warm surface water causes a decrease in surface density (PW).<\/figcaption><\/figure>\n

The profile above represents a stable state, or a high degree of stratification, where the warm, low density layer sits atop the colder, denser layer. If denser water happened to form at the surface, the water masses would be unstable, and the denser water would sink to the bottom, to be replaced by less dense water at the surface. This vertical movement of water masses based on density (as determined by temperature and salinity) is referred to as thermohaline circulation<\/a>, which is the topic of section 9.8<\/a>.\u00a0 By creating a stratified water column, the thermocline <\/a> and pycnocline <\/a> together create a barrier that prevents mixing between the warmer, less dense surface water and the colder, denser bottom water. In this way, nutrient-rich deep water may be prevented from coming to the surface to support primary production.<\/p>\n

As with temperature, there are also latitudinal differences in density. In the tropics the surface water is warm and low density, and there is a pronounced thermocline separating it from the colder, denser deep water. As stated above, this stratification prevents nutrient-rich water from reaching the surface and as a result tropical regions often have low productivity. In the high latitudes the water is uniformly cold at all depths, so there is little density stratification. The lack of a pycnocline (or a thermocline) allows cold, nutrient-rich deep water to more easily mix with the surface water, leading to higher primary production in polar regions.<\/p>\n

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