Private and Public Agencies

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Address the differences and similarities between public and private agencies, and their organizational structures and funding sources. This essay should expose to the many factors that influence how agencies function on a daily basis, from securing funding to selecting their model of service delivery. It should also emphasize on how systems theory is used when working with clients as well as how it influences operational structures of agencies.
Tasks:
Using online library, and the Internet, explore some of the differences in service delivery between private and public agencies. In your response, address the following:
•Identify several of the major differences in service delivery between private and public agencies. In your response, be sure to discuss the differences in the access to services, types of interventions, with special focus on systems theory, and organizational structures.
•Explain how these differences may affect the client or the patient. In your answer, elaborate on the benefits of a balanced system for clients and human services workers in the context of the operation of the agency.
•As a professional, discuss how your job might be affected by other direct service providers or mangers while working in these two settings.
•Discuss the factors affecting the everyday work of human services workers.

Homer

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Question:
Scholars vary in their dating of the Iliad and the Odyssey, which are attributed
to Homer (whether identified as a single individual or an accumulation of poets working under the name). Many scholars deem the written form of the poems to be the product of the eighth and sevenths centuries BCE and in many ways reflecting the social conventions of that period, but they also recognize that the poems had an oral basis that extended centuries earlier. In this sense, these texts represent how poets of the “Homeric age” were remembering Mycenaean palace societies from centuries before, but often in ways that conformed to contemporary experiences. Like the Hebrew book of Exodus, they reflect how people comprehended both present and past by contemplating how they related to each other.
For this assignment, contemplate Odysseus’ encounter with the Cyclops named Polyphemus amid his travels in the central Mediterranean (far from Troy and his home city of Ithaca, which are in the eastern Mediterranean). Why would Homeric poets of this time consider such memories of the remote past, as contained in the Odyssey 9, to be significant and compose a text or circulate oral traditions about them?
Your response should reflect consideration of the following issues:
a. Homeric social structures, morality, and reciprocity
b. the significance of culture and cultural difference for social or ethnic identities
c. the ideological implications of historical memories and the composition of history
?Formatting: 1-­-1.5 pages, New Times Roman, double-­-spaced, normal margins
Structure:
First Paragraph: Thesis and 2 Solid Supporting Arguments Second Paragraph: Supporting Argument 1
Third Paragraph: Supporting Argument 2
Citations: Provide specific citation of relevant passages of the Odyssey in your text, either as part of a sentence [“According to the Odyssey 9.115-­-142…”] or as a
???parenthetical insert [“…then Odysseus explored the new land that he encountered (Odyssey 9.115-­-142)”]
Books and Lines: book.line (Odyssey 9.115 is book 9, line 115)
?The link of Odyssey:
http://www.poetryintranslation.com/PITBR/Greek/Odhome.htm
Also, here is the information from the PPT that our teacher put on the web, please focus on it because the last assignment has lots of information from it.
Why Do Western Civ. Courses Treat Palace Societies as Origins of Western Civilization?
Is anything about them distinctly “western?” Is anything about them meaningfully distinct from Near Eastern societies.
To have “western civilization,” we need to define the beginning of “civilization”
?The Eastern Mediterranean and its Interconnected Systems during the “Bronze Age”: 1700-1200
1. Empires: Egypt and the Hittite Empire (in Turkey)
3. The regions are inhabited by various peoples (Minoans, Myceneans) in “palace societies.” No Greeks.
4. Some of these people may define themselves in regional terms as “Achaean.”
Great Online Resource for Aegean Prehistory:
FOR MORE INFORMATION ON THIS PAPER VISIT……
?
?From Gangs to “Palace” Societies People in regions that do not produce sufficient
agrarian wealth tend to be organized into “gangs”: a. Familial bonds: families share wealth
b. Patron-client relationships: people/families with resources have followers
c. Gangs fight or negotiate with other gangs
?Palace Societies
In parts of the (pre-)Greek world that have sufficient agrarian resources, gangs give way to “palace” societies:
a. Farmers produce excess food.
b. Successful gang leader takes excess food and
redistributes it to followers
c. Gang leader and his family uses wealth and power to:
a. Pay soldiers
b. Pay administrators
c. Organize religious practice
?Basic Chronologies
1. Minoans: c. 2700 BCE-1500 BCE
a. Crete, Aegean islands
b. Contacts and cultural exchange with Egypt and Canaanites of the Levant
?Basic Chronologies
Mycenaeans: 1700-BCE-1200 BCE
a. Sites at Greek mainland, Crete, Aegean Islands, Turkey, and other places
b. Trade with Hittite kingdom, the
Levant, and Egypt (shipwreck of south coast at Cape Gelidonya, Turkey c. 1200 BCE)
Mycenaean palace societies:
?Palace Societies: Tributary/Redistributive Economies
a. Palaces and their bureaucracies serve as centers of collection and redistribution of wealth for a wider agrarian society.
b. Palace societies have diplomatic and commercial contact with each other.
?Palace Societies
The following features of “palace” societies distinguish them from “gangs.”
a. Royal figure with religious charisma b. Royal succession
c. Writing (Linear A and Linear B)
d. Administration and standing army
*When gang leaders take from peasants, its plunder. When kings take from peasants, its “tribute” or “tax.”
?Linear B and Homer
1. (w)anax: royal figure
2. basileus: chief administrator
3. Megaron: room of a palace
System Failures
-So long as the Hittite kingdom, Egyptian kingdom, and palace societies maintain internal stability and interconnectivity, the Mediterranean world is stable.
-This harmonious balance is fragile. The collapse of one system could destabilize other systems.
System Failures
1250 BCE-1200BCE see complete and utter collapse. Scholars attribute it to a host of different factors, all of which may contribute:
a. Foreign invaders (“Dorian” Invasions, Sea Peoples)
b. Civil wars
c. Natural Catastrophe/Climate Change
d. Organic system collapse (system creates expanded bureaucracy and higher population, which it
eventually cannot support through collection and redistribution)

Do you think the members of Congress are fulfilling the job they were elected to do

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The actions, or some may say the inactions, of Congress have dominated the news recently. If you are not aware of the current budget and debt ceiling crises, just go to your favorite news source and learn more. Also, last week the presidents of every state run university in Utah signed a document urging Congress to take action on immigration reform because as of yet, nothing has come out of Washington.
Now read the views of Ezra Klein and Lee H. Hamilton in Issue 7 of Taking Sides “Is Congress a Dysfunctional Institution?” Also read the attached articles concerning Congress.
For this essay I want you to answer the question, “Do you think the members of Congress are fulfilling the job they were elected to do?”
demonstrate that you have read and understood the assigned readings. You will do so by utilizing those readings in your essay. Also, feel free to incorporate any outside material. If you do so, please be sure to properly cite that material.

CHILD PSYCHOLOGY/BEHAVIORISM

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Bandura, A., Ross, D., & Ross, S. A. (1961). Transmission of aggression through imitation of
aggressive models. Journal of Abnormal and Social PsychoQg{y, 63, 575-582.
wbobo.htm (ATTACHED“)”.r,)
m………__.__,__,J.//5
How do I write the paper?
Reading the Article:
0 You will probably need to read the article more than once to truly understand it.
0 You should pay attention to the main topic of the paper, what kinds of questions the
authors ask, how the ideas in the paper are organized, and what the tables, charts, and
graphs show.
0 It is best to take notes while you are reading the paper.
Content:
0 Your goal is to write a summary of the article that is so clear that a classmate could
understand it. In other words, your summary should show that you have read the article
carefully and understand the content of the article. Your paper should be a summary of
each of the following:
o The topic(s) of the study-What is the study fig?
o The goal(s) of the study-What is the question or questions at the heart of the article?
What questions are the authors trying to answer?
0 Who were the participants (subjects) in the study? Where did they come from?
o What answers did the authors find to their questions? In other words, what were the
results of the study?
0 What is E evaluation of this study? Are the results of this study important in the
real world? Would the results of this study change the way we do things in some area
of psychology?
Your paper does not need to go into the specific details of the data analysis/statistical techniques
used in the paper. You should check your paper for grammar and spelling.
You mpg’; describe the study in your own words, and you cannot quote directly from the text.
Any report that is entirely or partly copied word-for-word from a research article will
automatically be rated as a “fail” paper. That is plagiarism, and we do check for it.

Adolescent development paper

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Is the experience of being an adolescent the same for males and females? Is it the same across different historical time periods? What about across different cultures? This assignment involves exploring similarities and differences in these areas. Using the UOPX library, search for articles that address developmental changes in adolescence.
•Write a 1000-1500 word paper summarizing results from the research studies you have found. Your paper should include a brief introduction that includes a clear statement of purpose, a review of the research findings, your analysis of the research results, and a conclusion that summarizes the main points.

•Highlight a case study of one particular teenager, emphasizing real experiences that demonstrate success and or delay in developmental areas. 

•Include at least 3 references from professional peer-reviewed journals from the University of Phoenix library.
•Format your paper according to APA standards.
FOR MORE INFORMATION ON THIS PAPER VISIT……

depressive disorders

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1. How does disruptive mood dysregulation disorder differ from bipolar disorder in children?
2. What is the difference between Premenstrual Dysphoric Disorder and PMS?
3. What are the primary nonpharmaceutical and pharmaceutical treatments for enuresis?
4. What type of family system do children with encopresis typically have?
5. Case Study: Melissa
Melissa is a single, white, 14 y/o female, who is currently an 8th grade student. She was referred by the psychiatrist at St. Clare?s Hospital for medication management. She was recently released after a 10-day psychiatric inpatient stay where she was admitted for out-of-control behavior, severe temper outbursts, irritability, and severe conflict with friends and family.
Melissa began having problems about 5 years ago. She had a bullying incident the second week of school in third grade when a group of girls stole her jacket and threatened to beat her up. Although the girls were suspended, she was so distraught that she missed 7 days of school. She was unable to regain her equilibrium and catch up academically. By the end of December, she began experiencing symptoms of irritability, sadness, and mood swings. On Christmas Eve, 2012, she had a ?major meltdown? of explosive anger over not getting a new electronic device that she wanted. When her father refused to purchase it for her, she wouldn’t get into the car to return home and started screaming uncontrollably at him in the parking lot. Someone called the police and she was taken to St. Clare’s emergency room but was released after she calmed down.
After returning to school in January, she had difficulty concentrating and began having academic problems as well as relationship difficulties with her friends. She began having more conflict with her parents as well. After a family fight in March, 2011, following a limit setting attempt by her parents regarding time on the computer, she took an overdose of her sister’s medication (quetiapine and lamotrigine). She was admitted to St. Clare’s hospital for 11 days and then started their IOP program 3 times per week for 6 weeks. She had some improvement at home and at school. In May, however, she sent an inappropriate, seductive text picture to a boy she met on-line dressed in only her underwear. When her mother discovered this and confronted her, she broke glass and cut herself and took an overdose of 15 Advil. She was again admitted to St. Clares’ for 14 days. After discharge she started their PHP from 8:00 am to 3:30 pm, for the rest of the school year. There, she worked on developing better coping skills. The summer was uneventful and she started off her sophomore year on a positive note. After the first week, she started a relationship with a high school senior. After having her first sexual relationship with him, he soon broke up with her. She then, cut herself about 20 times on both forearms with a sharp knife and was readmitted to St. Clare?s for 5 days. She was released two days ago.
Currently, Melissa is still sad about the breakup with her boyfriend. She believes that she is unlovable and no one will ever want her. She is tearful and irritable and has difficulty concentrating. She admits to feelings of worthlessness, self-dislike, and pessimism. She states that sometimes her mood goes up and she feels on top of the world, but this happens infrequently. She has no difficulty sleeping and her appetite is good. She admits to having a terrible temper. There is no history of substance use. She also revealed that the sexual experience was very negative for her and her boyfriend wanted her to do ?lots of things? that he saw girls doing to men on internet porn and when she wouldn?t, he said he would find someone who would.
Melissa is currently on the following medication: Aripiprazole 5 mg; Intuniv 1 mg QAM; Doryx 150 mg HS (acne). In 4th grade her pediatrician thought she might have ADHD and was prescribed a low dose of Concerta but developed heart palpitations. She went for a cardiac evaluation and had increased PQ waves and a heart sequencing problem, so the Concerta was d/c and she was placed on Intuniv 1 mg, but she believes it doesn?t do anything for her and that she doesn?t have ADHD. Melissa is 5 ft, 7 inches; weight 124; BP 96/60. She has a mild case of acne.
Melissa was domestically adopted at 6 days from a single mother from Kentucky. She apparently had no psychiatric or medical history. Her father is a health care consultant and her mother a homemaker. There is no history of psychiatric problems. They appear to be good parents with appropriate parenting skills and without structural pathology in the family system. Melissa has a good relationship with them. Melissa has one sibling, Michelle, a 19 y/o sister who is also domestically adopted (no biological relationship). Michelle is diagnosed with Bipolar Disorder and is a freshman at Fairleigh Dickinson University, majoring in psychology. Michelle has had 3 psychiatric admissions and is currently stable and functioning well on Lithium 1200 mg/day.
Melissa is an accomplished ice skater and skates semiprofessionally. She has one good friend but their relationship is very conflictual. She is involved in community service for the homeless. She loves Face Book and other social media. Her family is middle to upper middle class and they own a farm in Tewksbury with a few horses.
Melissa is open and cooperative and looks her stated age. She is attractive with long blond hair, large green eyes, and mild acne. Her speech, communication, and behavior are normal. Her affect is appropriate and her mood is mildly labile moving from tearfulness to irritability during the evaluation. There is no indication of suicidal or homicidal ideation. Her thoughts are logical and goal directed. Her cognition is unimpaired. Her judgment and insight are fair.
Psychological Testing: A Young Mania Scale reveals a score of 7, indicating mild symptoms of bipolar disorder, but not enough to warrant a categorical diagnosis. A Beck Depression Inventory reveals a score of 10 indicating mild depression. A child study team evaluation report revealed two WISC scores different scores: scores at age 10 and 14 – went from FS IQ of 89 to 75, a VC from 91 to 87, PC from 91 to 87, WM from 97 to 71, and PS from 94 to 78.
How would you diagnose and treat this client?
DSM-5 Diagnosis
Differential Diagnosis
Treatment Recommendations/Plan
Further Testing:
Psychotherapy:
Medication management:

Trend analysis

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Topic: Personal connections/relationships
You will work with a partner of your choice on this assignment. Identify and analyze a trend in the marketplace that reflects society or popular culture (some previously studied trends are listed below – you may select any trend on or outside of this list). Your trend should have some implications for marketing and advertising. Review your topic with Professor Clark. Only one team will study a trend.
Research this trend using available secondary research and literature and any published studies. Summarize your trend and support it with facts from at least 5 secondary sources (beyond product web sites). Then draw implications from your trend for marketing/advertising in five product or service categories. You may use 2-3 examples of products/services that already exist and support the trend, but at least 2 examples need to be opportunistic applications of your trend in new product/service categories.
You and your partner will give a Power Point presentation – ten minutes in length – using a laptop. Spend part of your time highlighting the trend, and then briefly review your 5 examples. Your presentation will be supported by one five-page double-spaced paper, which should include parenthetical (MLA) citations and a bibliography listing sources used. Please hand in a paper copy of your presentation.
(What we need to do in this project is Summarize your trend and support it with facts and 2 product, my teammate will do the rest part)

Trade Routes, Upwelling, & Tides

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Answer the following question in a short, coherent, well-written paragraph. Attach your essay as a Word document.
Please cite your references for this and all essays with a URL or proper MLA or APA bibliographic citation.You may use the APUS on-line library to look for scholarly sources. The textbook may be cited as well a reference for essay answers. Be careful that you do not create a "cut and paste" paper of information from your various sources.
Answer the following question…
A massive ice shelf (larger than the island of Jamaica) broke off of the Wendell/Wilkens Ice Shelf on the Antarctic Peninsula. Looking at the current map on page 193 project where it might go in say the next 6 months. Also review the attached power-point on Antarctica and the arcticle about drilling into Antarctica’s buried lakes both are awesome.
1. estimate the density of a mixture of two samples of seawater that
have the same density but different temperatures and salinities,
2. describe and sketch changes in the seasonal thermocline at
mid-latitudes through the year,
3. plot temperature and salinity as a function of depth and identify
the thermocline and halocline,
4. list five different water masses and describe how they form,
5. relate surface convergence and divergence to downwelling
and upwelling,
6. describe the properties of water masses in each ocean basin,
7. describe and sketch the motion of water in the Ekman layer,
8. diagram the formation of surface current gyres,
9. locate the major surface currents on a map of the ocean basins,
10. explain the process of western intensification,
11. relate patterns of surface convergence and divergence to
downwelling and upwelling, and
12. sketch the Great Ocean Conveyor Belt.
CHAP T E R OUT L INE
7.1 Ocean Structure 182
7.2 Thermohaline Circulation and
Water Masses 186
7.3 The Layered Oceans 189
7.4 What Drives the Surface Currents? 191
7.5 Ocean Surface Currents 193
7.6 Current Characteristics 197
7.7 Eddies 199
7.8 Convergence and Divergence 200
7.9 The Great Ocean Conveyor Belt 204
7.10 Changing Circulation Patterns 204
Diving In: Ocean Drifters 207
7.11 Measuring the Currents 206
Summary 210
Key Terms 211
Study Problems 211
Ocean Structure
and Circulation
Sea surface temperature (SST) simulation created by scientists at the
National Oceanic and Atmospheric Administrationfs Geophysical Fluid
Dynamics Laboratory using a coupled atmosphere-ocean model.
Currents and eddies off the southern tip of Africa are evident.
182
E arth is surrounded by two great oceans: an ocean
of air and an ocean of water. Both are in constant
motion, driven by the energy of the Sun and the
gravity of Earth. Hidden below the oceanfs surface is its
structure. If we could remove a slice of ocean water in the
same way we might cut a slice of cake, we would find that,
like a cake, the ocean is a layered system. The layers are
invisible to us, but they can be detected by measuring the
changing temperature and salt content, and by calculating
the density of the water from the surface to the ocean floor.
This layered structure is a dynamic response to processes that
occur at the surface: the gain and loss of heat, the evaporation
and addition of water, the freezing and thawing of ice, and
the movement of water in response to wind. These surface
processes produce a series of horizontally moving layers of
water, as well as local areas of vertical motion. Surface currents
carry heat from one location to another, altering Earthfs
surface temperature patterns and modifying the air above. The
interaction between the atmosphere and the ocean is dynamic;
as one system drives the other, the driven system acts to alter
the properties of the driving system.
In this chapter, we will study both the surface processes
and their below-the-surface results in order to understand why
the ocean is structured and how its structure is maintained. We
will also explore the formation of the oceanfs surface currents.
We follow these currents as they flow, merge, and move away
from each other. We examine both horizontal and vertical
circulation, and consider ways in which they are linked to the
overall interaction between the atmosphere and the ocean.
7.1 Ocean Structure
Variation of Temperature
with Depth
With very few exceptions, the temperature
of seawater decreases with depth. Effectively
all of the energy available to heat the
ocean comes from incoming solar radiation.
Consequently, only a thin surface layer
of the ocean is heated directly because of
how rapidly solar radiation is absorbed with
depth (fig. 7.1). Nearly half of the total solar
energy at the sea surface is absorbed within
10 cm of the surface, and all of the infrared
energy is absorbed within about a meter of
the surface. A typical seawater temperatureversus-
depth profile consists of three gtemperature
layersh (fig. 7.2):
.3 .4 .5 .6 .7 .8 .9 1.0 1.1 1.2 1.3 1.4 1.5 1.6 1.7 1.8 1.9 2.0 2.1 2.2 2.3 2.4
Wavelength (10.4cm)
400
300
200
100
Visible part
Infrared
Surface
100 m
10 m
1 m
0.1 m
3%
20%
45%
60%
100%
Total Energy
Energy (arbitrary units)
Figure 7.1 A simplified plot of total solar energy in seawater as a function of depth. Area
below each curve is representative of the percent of available solar energy at the surface
that reaches that depth. A little over half of the total solar energy at the surface is absorbed
in the upper 1 m of water (only 45% penetrates to a depth of 1 m). Infrared energy is
absorbed particularly rapidly, with nearly all of it absorbed in the upper 1 m of water.
. a surface layer tens to a few hundreds of meters thick, called
the mixed layer;
. a region called the thermocline, extending from the bottom
of the mixed layer to a depth of about 1000 m (3280 ft); and
. the region from the base of the thermocline to the sea floor.
The mixed layer is an isothermal layer.a layer of constant
temperature. The thickness of the mixed layer is variable. It
depends on the depth to which the surface water is mixed by
turbulence caused by waves and wind. The mixed layer can be
as thick as 200.300 m (~650.1000 ft) at mid-latitudes in the
open ocean, whereas in protected coastal waters in the summer,
it can be as little as 10 m (~33 ft) thick. Between about 200.300 m
and 1000 m depth is the thermocline, where temperature
decreases rapidly throughout much of the ocean. This layer is
also frequently known as the gpermanent thermoclineh because
seasonal changes in climate at the surface do not influence water
temperature at these depths. Below 1000 m depth is the third,
and largest in volume, layer, which extends to the sea floor.This
deep water is nearly isothermal, temperature decreases very
slowly with depth, and it is uniformly cold everywhere. Roughly
75% of the water in the ocean has a temperature between 0 and
4‹C (table 7.1 and fig. 7.3). The discovery that the deep water
of the ocean, even in tropical regions, is very cold was made in
the eighteenth century. The obvious conclusion that followed
was that deep seawater must originate in polar regions, where
cold, dense surface water sinks and flows toward the Equator
along the ocean floor.
The details of actual temperature-versus-depth profiles
vary considerably depending on latitude and season of the year
(fig. 7.4). At mid-latitudes, the temperature and depth of the
mixed layer undergo seasonal changes with the formation of a
shallow seasonal thermocline in the summer and its disappearance
in the winter (fig. 7.4a). Throughout the winter, when strong
7.1 Ocean Structure 183
winds produce deep mixing and surface-water temperatures
are cold, the mixed layer may extend all the way to the top of
the permanent thermocline, producing an essentially vertical
temperature profile in the upper 200.300 m (fig. 7.5, March).
Throughout the summer, as surface temperatures rise and winds
decrease, the mixed layer will become more shallow and a
strong (steep temperature gradient) seasonal thermocline can
develop above the permanent thermocline (fig. 7.5, August).
At low latitudes, surface temperatures are warm and constant
throughout the year. Consequently, there is no development of
seasonal thermoclines and the three distinct temperature layers
are quite stable (fig. 7.4b). At high latitudes above about 60‹,
there is no permanent thermocline (fig. 7.4c). However, weak
seasonal thermoclines can develop in the summer. At high latitudes
there is often a layer of cold water 50.100 m below the
surface. Overall, the presence of three temperature layers in
the ocean is illustrated in the plot of seawater temperature in the
Pacific Ocean versus depth and latitude shown in figure 7.6.
Variation of Salinity with Depth
As discussed in chapter 5, the salinity of surface seawater
varies as a function of latitude in a relatively stable pattern
(review figs. 5.2 and 5.3). However, it is more difficult to draw
general conclusions about vertical profiles of salinity versus
depth. Depending on latitude, salinity may be relatively constant,
decrease, or increase with depth down to about 1000 m.
Below about 1000 m depth, the influence of surface processes is
minor and salinity is fairly constant. The total salinity range of
75% of the ocean is between 34.5 and 35.0 ppt (table 7.2 and
0
Mixed layer
Thermocline
Depth (m)
0 4 8 12 16 20 24
Temperature (‹C)
1000
2000
3000
4000
Figure 7.2 Simplified profile of temperature with depth in the
ocean. A shallow mixed layer with relatively constant temperature
overlies the thermocline, where temperature decreases rapidly with
depth. Beneath the thermocline, below a depth of about 1000 m,
temperature is fairly constant and cold.
Table 7.1 Distribution of Seawater Temperature
Temperature
Range (‹C)
Seawater Volume
(km3)
Percent of
Ocean Volume
.2.0 6409 4.7
0.2 57,990 42.4
2.4 40,065 29.3
4.6 11,849 8.7
6.8 6059 4.4
8.10 4222 3.1
10.12 2632 1.9
12.14 2358 1.7
14.16 1340 1.0
16.18 985 0.7
18.20 685 0.5
20.22 638 0.5
22.24 475 0.3
24.26 426 0.3
26.28 489 0.4
28.30 269 0.2
30.32 2 0.001
.2 0 2 4 6 8 10 12 14
Temperature (‹C)
km3
16 18 20 22 24 26 28 30 32
10,000
0
20,000
30,000
40,000
50,000
60,000 Figure 7.3 Distribution of seawater
temperature. Histograms indicate the
number of cubic kilometers of seawater
in each 2‹C range.
184 Chapter 7 Ocean Structure and Circulation
found at high latitudes. In either case, this marked
change in salinity with depth is called the halocline
(fig. 7.8). The general distribution of seawater salinity
in the Pacific Ocean is illustrated in the plot of
salinity versus depth and latitude shown in figure 7.9.
Variation of Density with Depth
Variations in temperature, salinity, and pressure
(depth) combine to control the density of seawater.
Seawater density is inversely proportional to temperature
and directly proportional to salinity and
pressure. This can be expressed as (ª = increases,
and « = decreases):
Density ª as temperature «
Density ª as salinity ª
Density ª as pressure ª
In general, variations in temperature and
salinity are more influential in determining seawater
density than are variations in pressure (or
depth). Consequently, we can consider density
to be a function of temperature and salinity. The
stratification of the ocean by temperature and
salinity that we have just discussed results in a
stratification of the ocean into density layers also.
A typical seawater density-versus-depth profile
consists of three gdensity layersh (fig. 7.10):
.. the mixed layer, a surface layer tens to a few hundreds of
meters thick;
0
Seasonal
thermocline
Permanent
thermocline
Permanent
thermocline
Midlatitudes Low latitudes
High
latitudes
Depth (m)
0 5 10 15 20
Temperature (‹C)
1000
500
1500
2000
2500
3000
0 5 10 15 20 25
Temperature (‹C)
.5 0 5
Temperature (‹C)
(a) (b) (c)
0
September
November
January
March May July August
Depth (m)
2 4 6 8 10 12 14 16
Temperature (‹C)
20
40
60
80
100
Figure 7.4 Simple temperature-versus-depth profiles for three latitude zones: (a) mid-latitudes with significant seasonal variation, (b) low latitudes
where climate tends to be uniformly warm through the year, and (c) high latitudes where climate tends to be uniformly cold through the year.
Figure 7.5 Detailed variation in the depth of the seasonal thermocline and the
temperature of the surface mixed layer at mid-latitudes. Solid lines indicate the
growth of the seasonal thermocline as it increases in strength and shoals during
the summer, and dashed lines indicate its decay as it becomes deeper and weaker
in winter. Note the different scales compared to figure 7.4.
fig. 7.7). In the upper 1000 m, areas where salinity decreases
with depth are typically found at low and middle latitudes
whereas areas where salinity increases with depth are typically
7.1 Ocean Structure 185
0 500 1000 1500 2000 2500 3000 3500 4000 4500 5000 5500 6000 6500 7000 7500 8500 9500
Distance (km)
8000 9000 10,000 10,500 11,000 11,500 12,000 12,500 13,000 13,500
1 2 3 4 5 6 7 8 9
33.0 34.0
< 33.0
> 36.5
35.0
Salinity
km3
36.0
1 2 3 4 5 6 7 8 9 1 2 3 4 5 6 7 8 9 1 2 3 4 5
0
10,000
20,000
30,000
40,000
Figure 7.6 Ocean temperature versus depth and latitude. North-south profile though the Pacific Ocean along the 150‹W meridian. Temperature
decreases with depth. The depth of the surface mixed layer and the permanent thermocline are less at low latitudes than at mid-latitudes because
winds are generally weaker and seasonal temperature contrasts are less at low latitudes. The black represents seafloor bathymetry.
Figure 7.7 Distribution of seawater salinity. Histograms indicate the number of cubic kilometers of
seawater in each 0.1 ppt range.
. a region called the pycnocline (which closely follows the
thermocline), extending from the bottom of the mixed layer
to a depth of about 1000 m (3280 ft); and
. the region from the base of the pycnocline to the sea floor.
QUICK REVIEW
1. What processes control the depth of the mixed layer?
2. Explain the difference between a seasonal thermocline
and the permanent thermocline.
3. How does the seasonal thermocline change during
the year?
4. Describe the basic characteristics of a temperatureversus-
depth profile at high latitudes, mid-latitudes,
and low latitudes.
5. Describe the total salinity range of seawater.
6. What is the halocline?
7. How does seawater density depend on temperature
and salinity?
186 Chapter 7 Ocean Structure and Circulation
7.2 Thermohaline Circulation
and Water Masses
Thermohaline Circulation
If the density of the water increases with depth, the water column
from the surface to that depth is stable. If there is higherdensity
water on top of lower-density water, the water column is
unstable. An unstable water column cannot persist; the denser
surface water sinks and the less-dense water at depth rises to
replace the water above it. When dense water from the surface
sinks and reaches a level at which it is denser than the water
above but less dense than the water below, it spreads horizontally
as more water descends. At the surface, water moves horizontally
into the region where sinking is occurring. The dense water
that has descended displaces deeper water upward, completing
the cycle. Because water is a fixed quantity in the oceans, it cannot
be accumulated at one location or removed at another location
without movement of water between those locations. This
concept is called continuity of flow. This motion, caused by
variations in density due to differences in temperature and salinity,
is called thermohaline circulation. Areas of thermohaline
circulation where water sinks are called downwelling zones;
areas of rising waters are upwelling zones. Downwelling is a
mechanism that transports oxygen-rich surface water to depth,
where it is needed for deep-living animals. Upwelling returns
low oxygen-content water with dissolved, decay-produced
nutrients to the surface, where the nutrients act as fertilizers to
Table 7.2 Distribution of Seawater Salinity
Salinity Range
(ppt)
Seawater Volume
(km3)
Percent of
Ocean Volume
<33.0 226 0.17
33.0.33.1 44 0.03
33.1.33.2 28 0.02
33.2.33.3 28 0.02
33.3.33.4 44 0.03
33.4.33.5 80 0.06
33.5.33.6 40 0.03
33.6.33.7 86 0.06
33.7.33.8 97 0.07
33.8.33.9 266 0.19
33.9.34.0 483 0.35
34.0.34.1 1058 0.77
34.1.34.2 1152 0.84
34.2.34.3 1896 1.38
34.3.34.4 4112 3.00
34.4.34.5 6515 4.76
34.5.34.6 12,301 8.98
34.6.34.7 44,235 32.31
34.7.34.8 32,761 23.93
34.8.34.9 7989 5.83
34.9.35.0 14,211 10.38
35.0.35.1 2396 1.75
35.1.35.2 1094 0.80
35.2.35.3 870 0.64
35.3.35.4 668 0.49
35.4.35.5 765 0.56
35.5.35.6 539 0.39
35.6.35.7 434 0.32
35.7.35.8 325 0.24
35.8.35.9 362 0.26
35.9.36.0 144 0.11
36.0.36.1 178 0.13
36.1.36.2 199 0.15
36.2.36.3 173 0.13
36.3.36.4 148 0.11
36.4.36.5 192 0.14
>36.5 786 0.57
0
High
latitudes
Low
latitudes
Halocline
Depth (m)
33 34 35 36 37
S/L
Increasing salinity (ñ)
1000
2000
3000
4000
Figure 7.8 Simplified profiles of salinity with depth in the ocean
for high and low latitudes. In each case, there is a surface mixed
layer of relatively constant salinity. Beneath the mixed layer at high
latitudes, salinity decreases rapidly to a depth of about 1000 m.
Beneath the mixed layer at low latitudes, salinity increases rapidly
to a depth of about 1000 m. The region of rapid change in salinity is
called the halocline.
187
Figure 7.10 Simplified profile of density with depth in the ocean.
A shallow mixed layer with relatively constant density overlies the
pycnocline, where density increases rapidly with depth (this layer
corresponds closely to the thermocline shown in figure 7.2). Beneath
the pycnocline, density increases slowly to the sea floor.
0 500 1000 1500 2000 2500 3000 3500 4000 4500 5000 5500 6000 6500 7000 7500 8500 9500
Distance (km)
8000 9000 10,000 10,500 11,000 11,500 12,000 12,500 13,000 13,500
0
Mixed layer
Pycnocline
Depth (m)
1.023 1.024 1.025 1.026 1.027 1.028
Density (g/cm3)
500
1000
1500
2500
2000
3500
3000
Figure 7.9 Seawater salinity versus depth and latitude. North-south profile through the Pacific Ocean along the 150‹W meridian. Most of
the variation in salinity is found in surface water with high values at low and middle latitudes and low values at high latitudes. Beneath about
1000.1500 m, salinity shows only minor variations. The black represents seafloor bathymetry.
promote photosynthesis and the production of more oxygen in
the sunlit surface waters. Upwelling and downwelling can also
be caused by wind-driven surface currents. When the surface
waters are driven together by the wind or against a coast, a
surface convergence is formed. Water at a surface convergence
sinks, or downwells. When the wind blows surface waters away
from an area or a coast, a surface divergence occurs and water
upwells from below. Surface convergences and divergences are
discussed further later in this chapter.
The speed of upwelling and downwelling water is about
0.1.1.5 m (0.3.5 ft) per day. Compare these flows to ocean
surface currents, which reach speeds of 1.5 m (5 ft) per second.
Horizontal movement at mid-ocean depth due to thermohaline
flow is about 0.01 cm (0.004 in) per second. Water caught in this
slow but relentlessly moving cycle can spend 1000 years at the
greater ocean depths before it again reaches the surface.
If the water column has the same density over depth, it has
neutral stability and is termed isopycnal. A neutrally stable
water column can easily be mixed vertically by wind, wave
action, and currents. If the water temperature is unchanging over
depth, the water column is isothermal; if the salinity is constant
over depth, it is isohaline.
Water Masses
There are many different combinations of temperature and
salinity that produce the same seawater density. This can be
illustrated in a temperature-salinity diagram, or T-S diagram,
where lines of equal density, or isopycnals, are drawn for many
combinations of temperature and salinity (fig 7.11). As the salinity
188 Chapter 7 Ocean Structure and Circulation
Figure 7.12 ARGO float measurements north of the Canary Islands
in the North Atlantic (about 31.37‹N, 25.27‹W) along vertical
profiles of (a) temperature and (b) salinity. (c) T-S plot of the data
collected can be used to identify specific water masses. Notice the
greater range of temperature and salinity found in surface waters
(red) compared to deep waters (violet).
Pressure (decibars)
2000
(a)
(b)
(c)
1500
1000
500
0
0 5 10 15 20 25
1 5 10 15 20 25
Temperature (‹C)
Cycle number/relative temperature
Float ID# 1900036
Pressure (decibars)
2000
1500
1000
500
0
34.5 35.0 35.5 36.0 36.5 37.0 37.5
1 5 10 15 20 25
Salinity (PSU)
Temperature (‹C)
5
0
10
15
20
25
2000 1500 1000 500 0
34.5 35.0 35.5 36.0
North Atlantic
central waters
Mediterranean water
Upper North Atlantic deep water
36.5 37.0 37.5
Pressure (decibars)
Salinity (PSU)
Cycle number/relative salinity
Surface waters
Temperature-Salinity Diagram
(lines of equal density in gcm.3)
Temperature (‹C)
20
15
10
5
0
33.5 34.0 34.5 35.0 35.5 36.0 36.5
Salinity ñ
A
B
75% A . 25%B
Mixture
50%A . 50%B
Mixture
75% A . 25%B
Mixture
50%A . 50%B
Mixture
25%A.75%B Mixture
Figure 7.11 The density of seawater, measured in grams per cubic
centimeter, is abbreviated as ƒÏ (rho) and varies with temperature
and salinity. Many combinations of salinity and temperature produce
the same density. Low densities are at the upper left and high densities
are at the lower right. The straight line is the mixing line for waters A
and B, both with the same density. A mixture of A and B lies on the
mixing line and is more dense than either A or B.
increases, the density increases; as the temperature increases, the
density decreases. Salinity can be increased by evaporation or
by the formation of sea ice; it can be decreased by precipitation,
the inflow of river water, the melting of ice, or a combination
of these factors.
FOR MORE INFORMATION ON THIS PAPER VISIT……
Any seawater sample can be plotted on a T-S diagram as a
single point and the density of the sample can be determined from
the isopycnals. Seawater samples from a common source that all
plot very near each other on a T-S diagram, with a narrow range
of temperature and salinity, define a water type. When two water
types (e.g, A and B in fig. 7.11) having the same density, but different
values of salinity and temperature, are mixed, they form a
new water type that lies on a mixing line (a straight line drawn
from point A to point B). The location of the new water type on
the mixing line will depend on the relative amounts of the two
original water types that were combined to form the mix. Notice
that the isopycnals are curved. Consequently, the mixture of two
water types with the same density will produce a new water type
with a density greater than either of the two original water types,
and the newly created mixed water will sink. This mixing and
sinking process is known as caballing and it occurs wherever
surface waters converge and mix.
A water mass is a large body of water that has similar
values of temperature and salinity throughout. Water masses
can be identified by measuring water temperature and salinity
along vertical profiles in the ocean and plotting these data on a
T-S diagram (fig. 7.12a and b). A water mass will be represented
on a T-S diagram by closely clustered data points (fig. 7.12c).
Surface-water masses typically have greater variability in temperature
and salinity than do deeper water masses.
7.3 The Layered Oceans 189
zone extends to 200 m (650 ft), and the intermediate zone lies
between 200 and 2000 m (1000 and 6500 ft). Deep water is
found between 2000 and 4000 m (6500 and 13,000 ft), and
bottom water is below 4000 m (13,000 ft).
The Atlantic Ocean
The properties of the layers of water making up the Atlantic
Ocean are shown in figure 7.13. At the surface in the North
Atlantic, water from high northern latitudes moves southward,
while water from low latitudes moves northward along the
coast of North America and then east across the North Atlantic.
These waters converge in areas of cool temperatures and high
precipitation at approximately 50‹. 60‹N in the Norwegian Sea
and at the boundaries of the Gulf Stream and the Greenland and
Labrador Currents. The resulting mixed water has a salinity of
about 34.9ñ and a temperature of 2‹. 4‹C. This water, known
as North Atlantic deep water (NADW), sinks and moves southward.
North Atlantic deep water from the Norwegian Sea moves
south along the east side of the Atlantic, while water formed
at the boundary of the Labrador Current and the Gulf Stream
flows along the western side. Above this water at 30‹N, a lowdensity
lens of very salty (36.5ñ) but very warm (25‹C) surface
water remains trapped by the circular movement of the major
oceanic surface currents. Between this surface water and the
North Atlantic deep water lies water of intermediate temperature
(10‹C) and salinity (35.5ñ). This water is a mixture of surface
water and the upwelled colder, saltier water from the subtropical
regions. It moves northward to reappear at the surface south of
the convergence in the North Atlantic.
QUICK REVIEW
1. Describe the concept of continuity of flow.
2. How do stable and unstable water columns differ?
3. What is the relationship between upwelling and
downwelling? Between surface divergence and convergence?
4. What is the difference between a water type and a
water mass?
5. Explain how water types with different temperature and
salinity can have the same density.
7.3 The Layered Oceans
Oceanographers have taken salinity and temperature measurements
with depth at many locations and for many years. Gradually,
they accumulated sufficient data to identify the layers of
water that make up each ocean and the surface source of the
water forming each layer. The structure of an ocean is determined
by the properties of these layers. Each layer received its
characteristic salinity, temperature, and density at the surface.
The waterfs density controls the depth to which the water sinks;
the thickness and horizontal extent of each layer are related
to the rate of its formation and the size of the surface source
region. Water that sinks from the surface to spread out at depth
and slowly mixes with adjacent layers eventually rises at another
location. In all cases, water that sinks displaces an equivalent
volume of water upward toward the surface at some other location
so that the oceansf vertical circulation is continuous.
The layers of water just described are associated with depth
zones: surface, intermediate, deep, and bottom. The surface
Africa
Surface water
36.5ñ
25 ‹C
Mediterranean
Outflow Water
Antarctic
Intermediate Water
Subantarctic
front
Antarctic
front
North Atlantic
Deep Water
Antarctic
Bottom Water
34.8ñ
.0.5 ‹C
34.9ñ
2.4 ‹C
35.5ñ
10 ‹C 34.2ñ
34.4ñ
34.6ñ
2 ‹C
5 ‹C
1
2
3
4
0‹
20‹ S
20‹ N
40‹ N
60‹ N
80‹ N
40‹ S
60‹ S
80‹ S
5
6
Depth (km)
Antarctica
surface convergence
surface divergence
Figure 7.13 North-south cross section of the
Atlantic Ocean illustrating major water masses
and their general movement. Areas of surface
convergence and divergence associated with
downwelling and upwelling are also shown.
190 Chapter 7 Ocean Structure and Circulation
the layers difficult to distinguish. Antarctic bottom water forms
in small amounts along the Pacific rim of Antarctica, but it
is quickly lost in the great volume of the Pacific Ocean. The
deeper water of the South Pacific Ocean is the water of the Antarctic
circumpolar flow. Because the North Pacific is isolated
from the Arctic Ocean, only a small amount of water comparable
to North Atlantic deep water can be formed. In the extreme
western North Pacific, convergence of the southward-flowing
cold water from the Bering Sea and the Sea of Okhotsk and
the northward-moving water from the lower latitudes produces
only a small volume of water that sinks to mid-depths. There is
no large source of deep water similar to that found in the North
Atlantic. Warm, salty surface water occurs at subtropical latitudes
(30‹N and 30‹S) in each hemisphere, and Antarctic intermediate
water is produced in small quantities, but its influence is small.
Deep-water flows in the Pacific are sluggish, and conditions are
very uniform below 2000 m (6600 ft). The slow circulation of
the Pacific means that it has the oldest water at depths where
age is measured as time from the waterfs last contact with the
surface. Residence time for deep water in the Pacific is about
twice that of deep water in the Atlantic.
The Indian Ocean
The Indian Ocean is principally an ocean of the Southern Hemisphere
and has no counterpart of the North Atlantic deep water.
Small amounts of Antarctic bottom water are soon mixed with
the deeper waters to form a fairly uniform mixture of Antarctic
circumpolar water brought into the Indian Ocean by the Antarctic
circumpolar current. There is a small amount of Antarctic
intermediate water, and in the subtropics, a lens of warm, salty
water occurs at the surface.
The Arctic Ocean
The Arctic Ocean basin is unique. About one-third of its area
is covered by extensive continental shelves, the widest of any
ocean basin. Two basins, the Eurasian to the east and the Canadian
to the west, occupy the central portion of the ocean; they
are separated by the Lomonosov Ridge extending due north
from Greenland.
The density of Arctic Ocean water is controlled more by
salinity than by temperature. Its surface layer is formed from
low-salinity water entering from the Bering Sea, fresh water
from Siberian and Canadian rivers, and seasonal melting of sea
ice. The surface layer from these combined sources is about
80 m (250 ft) deep and has a low salinity (32.5ñ) and a low
temperature (.1.5‹C). Below the surface layer, salinity increases
with depth in the halocline layer, 200 m (650 ft) thick, to reach
34.5ñ at its base. The cold, salty water of the halocline layer
is produced by annual freezing and formation of sea ice over
the continental shelves bordering the ocean. This water sinks
and moves across the shelves to spread out in the central ocean
basins. West of Spitsbergen, Norway, North Atlantic water (2‹C
and 35ñ) enters the Arctic Ocean and is cooled as it flows
under the halocline and fills the Arctic Ocean basins. This water
Near the equator, the upper boundary of the North Atlantic
deep water is formed by water produced at the convergence
centered
about 40‹S. This is Antarctic intermediate water
(AAIW). Because it is warmer (5‹C) and less salty (34.4ñ) than
the North Atlantic deep water, it is less dense and remains above
the denser and saltier water below. Along the edge of Antarctica,
very cold (.0.5‹C), salty (34.8ñ), and dense water is produced
at the surface by sea ice formation during the Southern Hemispherefs
winter. This is Antarctic bottom water (AABW), the
densest water in the oceans. This water sinks to the ocean floor
and flows slowly northward, creeping beneath North Atlantic deep
water, as it continues on through the deep South Atlantic ocean
basins west of the Mid-Atlantic Ridge. Antarctic bottom water
does not accumulate enough thickness to be able to flow over
the mid-ocean ridge system into the basins on the African side
of the ridge; it is confined to the deep basins on the west side of
the South Atlantic and has been found as far north as the equator.
At the same time, the North Atlantic deep water between
the Antarctic bottom and intermediate waters rises to the oceanfs
surface in the area of the 60‹S divergence. As it reaches the surface,
it splits; part moves northward as South Atlantic surface
water and Antarctic intermediate water; part moves southward
toward Antarctica, to be cooled and modified to form Antarctic
bottom water. A mixture of North Atlantic deep water and
Antarctic bottom water becomes the circumpolar water for the
Southern Ocean that flows around Antarctica. The Antarctic
circumpolar water becomes the source of the deep water found
in the Indian and Pacific Oceans. In this way, the Atlantic Ocean
and its circulation play a defining role in the structure and circulation
of all the oceans.
Warm (25‹C), salty (36.5ñ) surface water in the South
Atlantic
is also caught by the circular current pattern at the
surface and is centered about 30‹S. South of the southern tips
of South America and Africa, the water flows eastward, driven
by the prevailing westerly winds, which move the water around
and around Antarctica.
Water from the Mediterranean Sea has a temperature of about
13‹C and a salinity of 37.3ñ as it leaves the Strait of Gibraltar.
This water, mixing with Atlantic Ocean water, forms an intermediate
density water, Mediterranean Intermediate Water (MIW),
also known as Mediterranean Outflow Water (MOW), that sinks in
the North Atlantic to a depth of approximately 1000 m (3300 ft).
The influence of Mediterranean water can be traced 2500 km
(1500 mi) from the Strait of Gibraltar before it is lost through
modification and mixing.
FOR MORE INFORMATION ON THIS PAPER VISIT……
Because the Atlantic Ocean is a narrow, confined ocean of
relatively small volume but great north-south extent, the water
types are readily identifiable and the movement of the layers can
be followed quite easily. In addition, the bordering nations of the
Atlantic have had a long-standing interest in oceanography, so
the vertical circulation and layering of the Atlantic are the most
studied and the best understood of all the oceans.
The Pacific Ocean
In the vast Pacific Ocean, waters that sink from relatively small
areas of surface convergences lose their identity rapidly, making
7.4 What Drives the Surface Currents? 191
7.4 What Drives the
Surface Currents?
When the winds blow over the oceans, they set the surface water
in motion, driving the large-scale surface currents in nearly
constant patterns. The density of water is about 1000 times
greater than the density of air, and once in motion, the mass of
the moving water is so great that its inertia keeps it flowing.
The currents flow more in response to the average atmospheric
circulation than to the daily weather and its short-term changes;
however, the major currents do shift slightly in response to seasonal
changes in the winds. The currents are further modified by
interactions between the currents and along zones of converging
and diverging water. The major surface currents have been called
the rivers of the sea; they have no banks to contain them, but
they maintain their average course.
Because the frictional coupling between the ocean water
and Earthfs surface is small, the moving water is deflected by
the Coriolis effect in the same way that moving air is deflected
(see chapter 6). But because water moves more slowly than air,
it takes longer to move water the same distance as air. During
this longer time period, Earth rotates farther out from under the
water than from under the wind. Therefore, the slower-moving
water appears to be deflected to a greater degree than the overlying
air. The surface-current acted upon by the Coriolis effect is
deflected to the right of the driving wind direction in the Northern
Hemisphere and to the left in the Southern Hemisphere. In
the open sea, the surface flow is deflected at a 45‹ angle from
the wind direction, as shown in figure 7.14.
upwells along the edge of the continental shelves, mixing with
the water formed during freezing, and exits the Arctic as water
of 0.5‹C temperature and 34.9ñ salinity along the edge of the
shelf adjacent to Greenland. This exiting water moves south
along the coast of Greenland and enters the North Atlantic south
of Greenland and Iceland, where it combines with Gulf Stream
water to form North Atlantic deep water.
Internal Mixing
Mixing between waters in the ocean is most active when turbulence
and energy of motion are available to stir the waters and
blend their properties. At the sea surface, wind-driven waves and
currents supply energy for mixing, and the tides create currents
at all depths. The large eddies that may form at the boundaries of
currents also stir together dissimilar waters, acting to homogenize
them. When surface currents coverage, mixing at current boundaries
may produce caballing of the mixed water. When currents
and their associated turbulence are weak, mixing is reduced.
Mixing by diffusion occurs continually at the molecular level,
but diffusion is much weaker than mixing by turbulent processes.
If a parcel of water is displaced vertically by turbulence,
buoyancy forces tend to return the parcel to its original density
level. Therefore, vertical mixing between the water types that
form the oceansf internal layers is weak. Horizontal mixing is
more efficient because it requires less energy than vertical mixing.
A parcel of water displaced horizontally along a surface of constant
density remains at its new position and shares its properties
with the surrounding water.
In areas under warm, high-salinity surface water with an
appreciable salinity and temperature decrease with depth,
internal vertical mixing processes occur despite the stability
of the water column. Vertical columnar flows, approximately
3 cm (5 in) in diameter, are called salt fingers; they develop
and mix the water vertically, causing a stair-step salinity and
temperature change with depth. This phenomenon is caused by
the ability of seawater to gain or lose heat faster by conduction
than it gains or loses salt by diffusion. This causes the density
of the vertically moving water to change relative to that of
the surrounding water, and the moving water is propelled either
up or down. Salt fingers mix water over limited depths, creating
homogeneous layers 30 m (100 ft) thick. These layers exist
from about 150.700 m (500.2300 ft) deep and are estimated
to occur over large areas of the oceans when the required
conditions are present.
QUICK REVIEW
1. Identify the water masses of the Atlantic Ocean. What is
the origin of each? In which direction does each flow?
2. Why is the layering of the Pacific Ocean less dramatic than
the layering of the Atlantic Ocean?
3. In what ways is the water of the Indian Ocean similar to
the water of the South Atlantic Ocean?
4. What is the origin of Arctic Ocean deep water?
Wind stress
10 m
20 m
30 m
40 m
50 m
60 m
70 m
80 m
90 m
100 m
Each layer
drags the
layer below
45‹
Current speed
and direction
Mean direction
and flow
Figure 7.14 The Ekman spiral and Ekman transport. Water motion
in the surface gEkman Layerh is due to wind stress.
192 Chapter 7 Ocean Structure and Circulation
The Ekman Spiral and Ekman Transport
Wind-driven surface water sets the water immediately below it
in motion. But because of low-friction coupling in the water, this
next deeper layer moves more slowly than the surface layer and
is deflected to the right (Northern Hemisphere) or left (Southern
Hemisphere) of the surface-layer direction. The same is true for
the next layer down and the next. The result is a spiral in which
each deeper layer moves more slowly and with a greater angle
of deflection to the surface flow (fig. 7.14). This current spiral is
called the Ekman spiral, after the physicist V. Walfrid Ekman,
who developed its mathematical relationship. The spiral extends
to a depth of approximately 100.150 m (330.500 ft), where the
much-reduced current will be moving in the opposite direction
to the surface current. The surface layer of water corresponding
to the Ekman spiral is known as the Ekman layer. Over the
depth of the spiral, the average flow of the water set in motion
by the wind, or the net flow, moves 90‹ to the right (Northern
Hemisphere) or left (Southern Hemisphere) of the surface wind.
This is known as Ekman transport. This relationship is in
contrast to the surface water, which moves at an angle of 45‹ to
the wind direction.
Ocean Gyres
The major surface currents in the ocean are driven primarily
by the trade winds, blowing in a westerly direction toward the
equator, and the westerlies, blowing in an easterly direction
away from the equator (review figure 6.20). Surface water is
driven at a 45‹ angle to the direction of these winds (fig. 7.15).
Thus, the trade winds drive surface currents that flow from
east to west on either side of the equator. When these currents
reach the western boundaries of ocean basins, they are deflected
away from the equator and move to higher latitudes
where they enter the region of the westerlies. Once
under the influence of the westerlies, the surface
currents are then driven back across the ocean
basins from west to east. When these eastwardflowing
currents reach the eastern boundaries of
the ocean basins, they are largely deflected back
toward the equator where they again come under
the influence of the trade winds. This completes a
full cycle of surface currents that rotate clockwise
in the Northern Hemisphere and counterclockwise
in the Southern Hemisphere. These large, circularmotion,
wind-driven current systems are known
as gyres (fig. 7.16). In high southern latitudes,
no land separates the Atlantic, Pacific, and Indian
Oceans; here, the surface currents, driven by the
westerlies, continue around Earth in a circumpolar
flow around Antarctica.
Geostrophic Flow
Because of Ekman transport, a portion of the
wind-driven surface water
is deflected
toward the
center of each of the large, circular current
gyres
S
Elevated convergence
N
Elevated convergence
40‹N
30‹N
0‹
W E
30‹S
Winds Ekman
transport
Resulting
surface currents
40‹S
Northeast
trades
Southeast
trades
Westerlies
Westerlies
Doldrums
Tropical
divergence
a
b
d
c e
Figure 7.15 Wind-driven transport and resulting surface currents
in an ocean bounded by land to the east and to the west. The currents
form large oceanic gyres that rotate clockwise in the Northern
Hemisphere and counterclockwise in the Southern Hemisphere.
Figure 7.16 There are five major ocean gyres: (a) Indian Ocean, (b) North Pacific,
(c) South Pacific, (d) North Atlantic, and (e) South Atlantic gyres. Each has a strong and
narrow gwestern boundary current,h and a weak and broad geastern boundary current.h
just described (fig. 7.16). A convergent lens of surface
water
is
elevated as much as 2 m (6.5 ft) above the equilibrium
sea level,
and this lens depresses the underlying denser water.
7.5 Ocean Surface Currents 193
7.5 Ocean Surface Currents
The currents that make up the large oceanic gyre systems and
other major currents have been given names and descriptions
based on their average positions. These are presented here ocean
by ocean and can be followed on figure 7.18. As you follow
these current paths, review their associations with the large gyre
systems and their overlying wind belts.
Pacific Ocean Currents
In the North Pacific Ocean, the northeast trade winds push
the water toward the west and northwest; this is the North
Equatorial Current. The westerlies create the North Pacific
Current, or North Pacific Drift, moving from west to east.
Note that the trade winds move the water away from Central
and South America and pile it up against Asia, whereas the
westerlies move the water away from Asia and push it against
the west coast of North America. The water that accumulates in
one area must flow toward areas from which the water has been
removed. This movement forms two currents: the California
Current, moving from north to south along the western coast of
North America, and the Kuroshio Current, moving from south
to north along the east coast of Japan. The Kuroshio and California
Currents are not wind-driven currents;
they provide continuity of flow and complete
a circular motion centered around
30‹N latitude. This circular, clockwise
flow of water is called the North Pacific
gyre. Other major North Pacific currents
include the Oyashio Current, driven by
the polar easterlies, and the Alaska Current,
fed by water from the North Pacific
Current and moving in a counterclockwise
gyre in the Gulf of Alaska. Little
exchange of water occurs through the
Bering Strait between the North Pacific
The thickness of the surface lens is about 1000 times greater
than the elevation of the lens above sea level. This is because the
difference in density between the surface water and the deeper
water is only about 1/1000 of the density difference between
air and water at the sea surface. The surface slope of the mound
increases as deflected water moves inward until the outward
pressure driving the water away from the gyre center equals the
Coriolis effect, acting to deflect the moving water into the raised
central mound. At this balance point, geostrophic flow is said
to exist, and no further deflection of the moving water occurs.
Instead, the currents flow smoothly around the gyre parallel to its
elevation contours. See figure 7.17 for a diagram of this process.
QUICK REVIEW
1. If a north wind blows across the sea surface, what
direction does the surface current flow in the Northern
Hemisphere? In the Southern Hemisphere?
2. What is the direction of Ekman transport in question 1?
3. Why is the sea surface elevated in the interior of the major
current gyres?
4. Why do gyres rotate in opposite directions in the two
hemispheres?
V
V Fc Fg
Deeper water
V
V V
V
V
Fc
Fc
Fc Fc Fc
Fc
Fg
F Fg F g g
Lens of accumulated
surface water
Figure 7.17 Geostrophic flow (V) exists around a
gyre when Fc, the inward deflection force due to the
Coriolis effect, is balanced by Fg, the outward-acting
pressure force created by the elevated water and
gravity. This example is of a clockwise gyre in the
Northern Hemisphere.
Oyashio BBeerriinngg Alaska
North Pacific
California
North Equatorial
North Equatorial
Equatorial Counter
Current
Equatorial Counter
Current Equatorial Counter
South Equatorial Current
South Equatorial
Brazil
Somali
Benguela
Equatorial Counter
Current
Eqquatorial
Benguela
Agulhas
South Equatorial
West
Australian
East Australian Peru
Gulf Stream
North Atlantic
Labrador
Norwegian
East
Greenland
Canary
Antarctic Circumpolar Antarctic Circumpolar
Kuroshio
Figure 7.18 The long-term average flow of
the major wind-driven surface currents.
194 Chapter 7 Ocean Structure and Circulation
ward movement of South Atlantic surface water across the
equator results
in a net flow of surface water from the Southern
Hemisphere
to the Northern Hemisphere. This flow is balanced
by a flow of water at depth from the Northern Hemisphere to the
Southern Hemisphere. This deep-water return flow is the North
Atlantic deep water. Again, the equatorial
currents are displaced
northward, although not as markedly as in the Pacific Ocean.
The Sargasso Sea marks the middle of an ocean gyre. It is
located in the central North Atlantic Ocean, and its boundaries
are the Gulf Stream on the west, the North Atlantic Current
to the north, the Canary Current on the east, and the North
Equatorial
Current to the south. The circular motion of the
gyre currents
isolates
a lens of clear, warm, downwelling water
1000 m (3000 ft) deep. The region is famous for the floating
mats of Sargassum,
a brown seaweed, stretching across its
surface. The extent of the floating seaweed frightened early
sailors, who told stories of ships imprisoned by the weed and
sea monsters lurking below the surface. Except for the floating
Sargassum, with its rich and specialized
ecological community,
the clear water is nearly a biological
desert.
Indian Ocean Currents
The Indian Ocean is mainly a Southern Hemisphere ocean. The
southeast trade winds push the water to the west, creating the
South Equatorial Current. The Southern Hemisphere westerlies
still move the water eastward in the West Wind Drift.
The gyre is completed by the West Australia Current moving
northward and the Agulhas Current moving southward
along the east coast of Africa. Because this is a Southern
Hemisphere ocean, the currents are deflected left of the wind
direction, and the gyre rotates counterclockwise. The northeast
trade winds in winter drive the North Equatorial Current to
the west, and the Equatorial Countercurrent returns
water
eastward toward Australia. Again, these equatorial currents
are displaced approximately
5‹N. With the coming of the wet
monsoon season
and its west winds, these currents are reduced.
The strong seasonal
monsoon effect controls the surface flow
of the Northern
Hemisphere portion of the Indian Ocean. In
the summer,
the winds blow the surface water eastward, and
in the winter, they blow it westward (fig. 7.19). This strong
seasonal shift is unlike
anything found in the Atlantic or the
Pacific Ocean.
Arctic Ocean Currents
The relentless drift of water and ice in the Arctic Ocean moves
in a large clockwise gyre driven by the polar easterly winds.
This gyre is centered not on the North Pole, as early explorers
expected,
but is offset over the Canadian basin at 150‹W and
80‹N (fig. 7.20). Although the currents and the winds move the
ice slowly at 0.1 knot (2 mi/day), Arctic explorers trying to reach
the North Pole found that they traveled south with the drifting ice
and water at speeds almost equal to their difficult progress north.
The Arctic Ocean is supplied from the North Atlantic
by the Norwegian Current; some of this flow enters west of
and the Arctic Ocean; no current exists that is comparable to the
Atlantic
Oceanfs Norwegian Current, which moves warm water
to the Arctic Ocean.
In the South Pacific Ocean, the southeast trade winds move
the water to the left of the wind and westward, forming the South
Equatorial Current. The westerly winds push the water to the
east. The current formed, the Antarctic Circumpolar Current, moves
continuously around Earth. The tips of South America
and Africa
deflect a portion of this flow northward on the east sides of the
South Pacific and South Atlantic Oceans. As in the North Pacific,
continuity currents form between the South Equatorial Current
and the Antarctic Circumpolar Current. The Peru Current, or
Humbolt Current, flows from south to north along the coast of
South America, while the East Australia Current can be seen
moving weakly from north to south on the west side of the ocean.
These four currents form the counterclockwise South Pacific gyre.
The North Pacific and South Pacific gyres form on either side
of 5‹N because the meteorological equator, or doldrums belt, is
displaced northward from the geographic equator (0‹), owingto
the unequal heating of the Northern and Southern Hemispheres.
Also between the North and South Equatorial Currents, in the
zone of the doldrums is a current moving in the opposite direction,
from west to east. This is a continuity current known as the
Equatorial Countercurrent, which helps to return accumulated
surface water eastward across the Pacific. Under the South Equatorial
Current is a subsurface current flowing from west to east
called the Cromwell Current. This cold-water continuity
current
also returns water accumulated in the western Pacific.
Atlantic Ocean Currents
The North Atlantic westerly winds move the water eastward
as the North Atlantic Current, or North Atlantic Drift. The
northeast trade winds push the water to the west, forming the
North Equatorial Current. The north-south continuity currents
are the Gulf Stream, flowing northward along the coast of
North America, and the Canary Current, moving to the south
on the eastern side of the North Atlantic. The Gulf Stream is
fed by the Florida Current and the North Equatorial Current.
The North Atlantic gyre rotates clockwise. The polar easterlies
provide the driving force for the Labrador and East Greenland
Currents, which balance water flowing into the Arctic Ocean
from the Norwegian Current.
In the South Atlantic, the westerlies continue the West Wind
Drift. The southeast trade winds move the water to the west, but
the bulge of Brazil deflects part of the South Equatorial Current
northward into the Caribbean Sea and eventually into the Gulf of
Mexico, where it exits as the Florida Current and joins the Gulf
Stream. A portion of the South Equatorial
Current moves south
of the Brazilian bulge along the western side of the South Atlantic
to form the Brazil Current. The Benguela Current moves
northward
along the African coast. The South Atlantic gyre is
complete, and it rotates counterclockwise.
Because much of the South Equatorial Current is deflected
across the equator, the Equatorial Countercurrent appears only
weakly in the eastern portion of the mid-Atlantic. The north195
Spitsbergen, but most flows along the coast of Norway and
moves eastward along the Siberian coast into the Chukchi Sea.
A small inflow of water entering the Arctic through the Bering
Strait brings water from the Bering Sea to join the eastward
flow along Siberia and the large Arctic gyre. The western side
of the gyre crosses the center of the Arctic Ocean to split north
of Greenland. Here, the larger flow forms the East Greenland
Current flowing south and taking Arctic Ocean water into the
North Atlantic. The lesser flow moves along the west side of
Greenland
to join the Labrador Current and move south along
the Canadian coast.
Outflow from Siberian rivers is caught in the eastward
flow of water and ice along Siberia. Eventually, this discharge
joins the gyre, distributing sediments and pollutants throughout
the Arctic.
Northeast Monsoon (January)
Southwest Monsoon (July)
H
H
INDIA
OMAN INDIA
North Equatorial Current
East Arabian
Current
South Equatorial Current
Southwest Monsoon Current
Somali Current
South Equatorial Current
Equatorial Countercurrent
Weak Equatorial
Countercurrent
SOMALIA
East African
Coastal
Current
SUMATRA
OMAN INDIA
SOMALIA
Weak Equatoria
Countercurrent
MOZAMBIQUE
Sout
MOZAMBIQUE
MADAGASCAR
t Monsoon (July)
So
MADAGASCAR
Equatorial Coun
MADAGASCAR
MOZAMBIQUE
SUMATRA
INDIA
L
L
H
L
Figure 7.19 Indian Ocean monsoonal circulation. In the winter, high pressure over the continent creates dry monsoon winds roughly out of
the northeast that drive water in the Northern Hemisphere portion of the ocean to the west. In the summer, low pressure over the continent
creates wet monsoon winds roughly out of the southwest that reverse the surface currents in the North Hemisphere portion of the ocean.
Figure 7.20 The circulation in the Arctic Ocean is driven by the
polar easterlies, which produce a large, clockwise gyre. Water enters
the Arctic Ocean from the North Atlantic by way of the Norwegian
Current and exits to the Atlantic by the East Greenland Current and
the Labrador Current.
East Greenland C.
Norwegian C.
West Greenland C.
Labrador C
.
Spitsbergen
90‹N
80‹
70‹
60‹
90‹W 90‹E
W0‹E
W180‹E
CANADA
SIBERIA
ALASKA
(U.S.)
GREENLAND
ICELAND
SWEDEN
FINLAND
NORWAY

Mapping The zeitgeist

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Use Nystrom’s framework to map the spirit of the times (1940’s) To sensitize yourself to this concept, map the zeitgeist using the categories of dominant events, ideals, social groups, attitude and technology for the 1940’s decade. Use Nystrom’s 2 elements for observing the zeitgeist as your guide. Please follow and answer the questions below. Please bullet point each topic.
1: Dominating events in 1940’s
A: what were the significant occurrences of the decade? PLEASE MAKE SURE TO INCLUDE; World events, war, death of world leaders. And etc,…
B: what was popular in art, music, entertainment, literature, fashion?
Include: Academy Awards. Emmy’s, Grammy’s NYT best seller list, and etc…
C: what were the discoveries of the decade
D: Were there any accidental events
Ex, Disasters, Accidental discoveries, King tut’s tomb
2: Dominating Technology
A: what technological advances were discovered during the time?
B: what were the impacts of society

‘synthesis’ of your contributions

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Topics
1. Language, dialects and varieties
2. Pidgin and creole languages
3. Language and Gender
4. Choosing a code
5. Code switching
6. Language and culture
7. Ethnography and Ethnomethodology
8. Linguistics etiquette
9. Multilingualism and language planning
10. Language planning and policy
Please note that this assessment requires that you provide a ‘synthesis’ of your contributions to discussion forums over the weeks leading up to the assignment date.
One approach could be a quick look at the online Collins English Dictionary (2003):
Synthesis
1. The process of combining objects or ideas into a complex whole Compare analysis
2. The combination or whole produced by such a process
This means that you have to bring together all the contributions you made in the forums and submit one whole analysis/narrative which reflects your understanding/experiences of the concepts under review. Avoid simply submitting a ‘cut and paste’ of their contributions to the forums. It is important that you demonstrate your ability to synthesis your understanding in a continuous and cohesive narrative.
Some students email questions to me directly and I would to encourage this practice if you do not get appropriate feedback from your peers on the study desk. However, please check that the issues has not already been answered in the discussion forums or by the course examiner before sending in an email..
Wishing you the best of luck with the next assignment.
3. Discussion Board Journal
Description
Discussion Board Journal (1000 words)
In this assignment you are required to show your leadership and participation in the Study Desk discussion forum presentations. As evidence of this you are required to follow study desk lectures and engage in forum discussions on each topic every week while noting down your beliefs and assumptions about each topic in a journal. This will allow you to reflect upon your learning, how it relates to the way you teach or have taught, and the extent and ways in which your own theories/views on Sociolinguistics undergo a change or deepen.
Your postings on the study desk and journal entries therefore become a record of your experiences, feelings and reflections on the literature as you undertake this course. Your feelings may vary from topic to topic but continuous reflection will assist deeper understanding of the concepts and learning. You are required reflect on classroom experiences you may have had, or demonstrate a higher level of appreciation of some of your previous experiences with language learning.
For this assessment you will be required to:
• First, copy and paste into a Word document selected sections of the discussion interactions from your own Study Desk presentation that best demonstrate your leadership of your discussion and your contribution to other forum discussions.
• Using these extracts from the study desk contributions and in a continuous narrative, write about your learning journey throughout the semester, reflecting on topics or concepts (at least five minimum) that challenged your thinking mostly and outline how this will impact on your future practice. Do not include subheadings or dates of entries.
• Submit this assignment through EASE.`
• Use APA referencing style.
• The 1000-word limit (with an allowance of 10% under or over) will be strictly applied in this assignment.
• The 1000-word limit includes all the chosen texts (including the highlighted text), the five things you have learned and in-text references. References at the end of the assignment are not included in the word count
Samples of various types of discussion journals
Sample 1 of a Discussion Journal
I have been thinking about my language behaviour in the classroom, with specific regard to the function of questioning (Brown &Wragg, 1993). I have come to realise that I often seem to (mis)interpret students’ silence as their not having understood my question. I tend to either ‘fill the gap’ in the conversation or rephrase the question. In retrospect I believe at least some of the time if I would only wait, the students could produce an appropriate, if not correct, answer. They have so much to cope with in learning English as an L2 that they simply need more time to form a response. I must try to be more patient with them while they are thinking.
Sample 2 of a Discussion Journal
Hypotheses proposed by Krashen (1983) regarding L2 learning contain a mixture of valid theories and not so valid ideas. All together the theory seems valid and on the surface appears to answer some of the questions regarding Second Language Learning (SLL). However not all the five hypotheses are of equal status in terms of ‘provability’ or even credibility as explanations for certain aspects of language learning or acquisition. The notion of an ‘affective filter’ is an interesting one – although of course it is not unique. I’m certain that affective features play a big part in SLL. Whether it is motivation, self-esteem and confidence, racial/ethnic problems or whatever, the affective area must either limit or assist a learner to acquire or learn the new language. I’m not altogether convinced that there is in fact any real difference between second language learning and second language acquisition but that the distinction is an arbitrary one made to distinguish the mode or means of learning the language. Surely whether it is learned in the classroom or in the street or workplace, it is still second language learning and the problems in understanding usage etc. are going to be the same or similar.
Sample 3 of a Discussion Journal
Anyway after all the readings I’ve done on the subject of bilingualism and cognition I think the threshold theory (Cummins, 1976) makes quite a bit of sense – surely there is a need for a level of competence in L1 in literacy skills to be attained before the student in the second language learning situation can achieve success – not necessarily in the oral part but in the reading and writing of the second language – I guess it makes sense.