How does our understanding of geology and plate tectonics improve our understanding of earthquakes? How does this understanding affect our lives (i.e. human settlement, etc.) and/or improve the quality of life for humans? Provide three examples. - Management
How does our understanding of geology and plate tectonics improve our understanding of earthquakes? How does this understanding affect our lives (i.e. human settlement, etc.) and/or improve the quality of life for humans? Provide three examples.
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INTRODUCTION TO EARTHQUAKES
An earthquake is the vibration of the earth produced by a release of energy
as a sudden movement of rock mass occurs along faults.
Earthquakes are very common geologic phenomena:
-over 800,000 earthquakes occur every year
-nearly all of these are very minor, too small to be felt by people
-but about 20 earthquakes of M=7.0 (the size of the 1989 Loma Prieta
earthquake) or larger occur around the world annually.
Large earthquakes are among the most destructive of natural phenomena.
-during historic times, earthquakes in populated areas have caused
50,000 or more deaths at least 16 times.
The most destructive historic earthquake occurred in China in 1556
-it is estimated that 830,000 people died
-one reason for the huge death toll was that people in the region lived
in cave dwellings excavated from bluffs of soft sediment, which
collapsed during the earthquake.
More recently, another large earthquake in China in 1976 killed at least
250,000 people
-some estimates as high as 700,000.
Because of their destructive power, scientists have studied earthquakes very
intently, with the hope of understanding their exact causes and
mechanisms of occurrence
-and to use this knowledge to find ways of predicting the location and
time of occurrence of large earthquakes.
Earthquakes have also provided earth scientists with a powerful tool for
studying the properties and structure of the earth's interior
-vibrations set up by large earthquakes propagate throughout the earth
-studies of the travel times and travel paths of these vibrations allow us
to determine the density and other physical properties of rocks
below the surface
-and how these properties vary with depth
-revealed the layered structure of the earth, with divisions into core,
mantle, and crust.
ORIGIN OF EARTHQUAKES: ELASTIC REBOUND
The way in which earthquake vibrations are generated was not understood
by geologists when the large 1906 earthquake struck San Francisco and
northern California.
During this earthquake, much of northern part of the San Andreas fault
ruptured: from Hollister northward to Cape Mendocino.
-the shaking lasted in San Francisco for 48 seconds.
-during this time, the crust west of the fault shifted northwestward
-horizontal offset at the fault reached as much as 6 m (20 ft) in Marin
County.
After the earthquake, studies revealed that strain had been building up in the
region surrounding the fault for a long time
- the evidence was found in land surveys made during the 50 years
preceding the quake
-the surveys showed that distant points on either side of the fault were
slowly being displaced during the decades prior to the quake
-the displacement was horizontal, parallel to the fault, as much as 3 m
(10 ft)
-but no movement occurred on the San Andreas fault itself during this
time: the fault was locked by friction
-displacement resulted from gradual deformation spread through the
rocks on either side of the fault, across a zone tens of km wide.
Survey lines crossing the fault were being bent by the build-up of strain in
the rocks surrounding the fault:
On the basis of this evidence, the Elastic Rebound mechanism of
earthquake generation was proposed.
This theory is based on the fact that when rocks are subjected to small,
temporary stress, they behave like elastic materials:
-they change shape temporarily
-but when stress is removed, they spring back to their original shape
-in effect, when elastic materials deform, they store up elastic energy,
which is released when stress is removed, and enables them to
return to their original shape.
The bending of rocks adjacent to a locked fault stores up elastic energy and
increases the stress along the fault
-eventually, stresses acting parallel to the fault exceed the friction that
prevents movement
-the fault suddenly slips, with movements as rapid as several meters in
a few seconds
-as the fault slips, the rocks adjacent to the fault suddenly "unbend",
and spring back to their original shape, releasing the stored elastic
energy
-the sudden motion of the unbending rocks generates the vibrations
that we feel as an earthquake.
The potential for earthquakes is greatest along active faults that are
temporarily locked
-the size of the earthquake is related to how long the fault has been
locked, how much elastic strain has built up, and how large a
portion of the fault slips.
The slip that occurs during a major earthquake may not relieve all of the
built-up stress:
-after a major quake, additional smaller offsets commonly occur along
faults
-these generate smaller earthquakes called aftershocks
-despite their smaller magnitude, aftershocks can do significant
damage because many structures may be badly weakened by the
main quake.
Major earthquakes may also be preceded by smaller quakes called
foreshocks
-monitoring faults for foreshocks is one strategy for earthquake
prediction.
SEISMIC WAVES
The vibrations produced by an earthquake radiate outward from the
earthquake focus in all directions
-the study of earthquake vibrations is called seismology
-and the instruments used to measure and record seismic vibrations are
called seismographs.
-the record of these vibrations is a seismogram.
Some earthquake energy sets up a wave-like disturbance of the earth's
surface: surface waves
-like the ripples on the surface of water
But most earthquake energy moves as body waves:
-waves that move through the rocks in the interior of the earth.
There are two types of seismic body waves:
-Primary or P-waves, also called compressional waves
-Secondary or S-waves, also called transverse waves.
P-waves
As P-waves travel through rock, the rocks oscillate back and forth in the
direction the wave is travelling
-rocks are alternately pushed and pulled in the direction of wave
motion
-or rocks are alternately compressed and expanded.
A P-wave can be simulated with a large spring
-if the spring is stretched, and you bunch the coils at one end
-when released, the zone of compression travels longitudinally down
the spring, followed by a zone of expansion.
Sound traveling through the air moves in this same way, as alternate
compressions and expansions of the air
-because solids, liquids, and gasses can all be compressed elastically,
P-waves can travel through all three phase states of matter.
S-waves
S-waves are what physicists call transverse waves:
-rocks oscillate back and forth at right angles to the direction of wave
travel
S-waves can be illustrated by tying one end of an elastic rope to something
and shaking the other end
-an S-wave travels down the rope and reflects back from the tied end
S-waves produce temporary changes in shape of the rocks which are
recovered as the waves pass
-S-waves propagate readily through rocks, but cannot be transmitted
through a liquid or gas (unlike P-waves)
-if you try to push a liquid sideways, it simply flows
-it does not spring back when the stress is removed
This difference between P-waves and S-waves allows us to determine which
parts of the earth's interior are solid and which parts are liquid.
Surface waves
The motion of surface waves is similar to that of S-waves, but the motion
dies out downward below the surface
-the ground surface oscillates back and forth at right angles to the
direction of wave travel
-both up-and-down and horizontal side-to-side motions occur in
different types of surface waves.
-when large shallow earthquakes occur, observers near the epicenter
can sometimes see the ground surface undulating up and down by
a meter or more as the surface waves pass.
Seismic Waves and Seismograms
How can we recognize different seismic waves on a seismogram?
-for earthquakes some distance away from a recording station, this
turns out to be fairly easy
-the different waves arrive at the seismograph at different times
-because the different wave types travel at different velocities.
The first wave to arrive is the P-wave: which is the source of the name.
-the P-wave is the fastest type of seismic wave
-the exact velocity depends upon rock type, rock density, and depth
-for granite at shallow depths in the crust, Vp = 6 km/sec
The S-wave is the second wave to arrive:
-it is significantly slower than the P-wave
-for granite, Vs = 3.5 km/sec
-for any rock type, the P-wave travels 1.7 times as fast as the S-wave.
The S-waves also usually have a higher amplitude than the P-waves
-the wiggles on the seismograph trace are more pronounced.
Surface waves are slightly slower than S-waves:
-travel at 0.9 times the velocity of S-waves
-so they are the last to arrive
-usually have much higher amplitudes than the body waves.
LOCATING EARTHQUAKES
The source of an earthquake is the point where a fault first begins to rupture
-this nearly always occurs some distance below the surface
-for many deeper earthquakes, the zone of rupture never reaches the
surface, and there may be no surface offset.
This point of origin of the earthquake waves is called the earthquake focus.
-the epicenter of an earthquake is the point on the earth's surface
directly above the focus.
The difference in velocity and arrival times of P-waves and S-waves
provides the data that allow earthquake epicenters to be located.
When an earthquake is recorded at a seismograph station, we don't initially
know the exact time at which the earthquake began
So we can't use the arrival time of the P-wave alone, for example, to
determine how far away the epicenter is.
But for any seismic station more than a few miles from the earthquake
epicenter, there will be a time lag between the arrival of the P and S
waves.
-as the waves radiate away from the epicenter, the slower S-wave lags
farther and farther behind the P-wave
-so the difference in arrival times increases with distance.
If both P and S-waves are recorded at our station, we can easily measure the
time lag between their first arrivals
-that time difference will correspond to a specific distance from the
epicenter.
Unfortunately, with a single seismograph station, we don't know the
direction from which the seismic waves were traveling.
But the epicenter must lie on a circle centered on the seismograph station,
with a radius equal to the calculated distance
In order to find the exact location of the epicenter, we must have distance
measurements from at least three seismograph stations
-the circles drawn around each station should all intersect in a single
common point: the epicenter.
For seismograph stations close to the epicenter, the depth of the earthquake
focus also affects the travel time of seismic waves
-seismic waves from a deep earthquake will take longer to reach a
nearby station than waves from a shallower earthquake
-travel-time data from a number of nearby seismic stations can be used
to establish the focal depth.
Earthquake foci vary in depth from 5 km to 700 km below the surface.
-seismologists have divided earthquakes into three depth ranges (which
are somewhat arbitrary)
-shallow earthquakes are less than 70 km deep.
-intermediate depth earthquakes are between 70 and 300 km deep.
-deep earthquakes are deeper than 300 km.
About 90% of all earthquakes are shallow-focus earthquakes.
-intermediate and deep earthquakes are exceptional, and played an
important role in working out the plate-tectonic theory.
EARTHQUAKE MAGNITUDE AND INTENSITY
Earthquakes vary greatly in strength and in the effects they produce at the
surface. Two different ways to compare the relative strength of
earthquakes are the magnitude and intensity.
Magnitude
The magnitude of an earthquake is a fairly objective measure of the strength
of an earthquake.
-is determined from the ground motions measured by seismic
instruments.
The basic assumption in magnitude measurement is that the amplitude of
seismic waves recorded on seismograms is related to the amount of
energy released in the earthquake
-the larger the earthquake, the greater the amplitude of the vibrations.
The technique for determining earthquake magnitude was developed by
Charles Richter and associates at Cal Tech in 1935
-the magnitude scale is now called the Richter Scale
Magnitude is determined by measuring the amplitude of the largest wave
recorded by a standard type of seismograph: this is usually the surface
wave.
-but seismic waves spread out and weaken as they move away from the
source
-the wave amplitude diminishes at more distant seismic stations
-so observed amplitudes are corrected for these variations due to
distance from the source
Because the size of earthquakes varies enormously, the amplitudes of ground
motions measured by seismographs differs by factors of thousands from
earthquake to earthquake.
-so to obtain a scale which expresses variations in amplitude in small
numbers, the Richter Scale is logarithmic
This means that an increase in Richter magnitude of 1.0 between two
earthquakes is equal to a ten-fold increase in wave amplitude
-a magnitude 5.0 earthquake has a wave amplitude 10 times that of a
magnitude 4.0 quake
-a magnitude 6.0 quake has an amplitude 100 times higher
-a magnitude 7.0 quake has an amplitude 1,000 times higher.
The smallest earthquakes that can be felt by people under ideal
circumstances are about magnitude 1.5
-damage to structures may occur at magnitudes greater than 4.5.
The Richter scale has no inherent upper limit
-but the largest earthquake magnitude that has been measured this
century is 8.9, in two earthquakes.
-this appears to represent a natural upper limit, related to the strength
of rocks in the crust.
Seismic wave amplitude correlates in a crude way with the amount of energy
released by an earthquake
-an increase in magnitude of 1.0 increases the amount of seismic
energy released by a factor of 30, not just 10.
-so a magnitude 6.0 earthquake releases 900 times more energy than a
magnitude 4.0 quake.
The largest earthquakes (over Magnitude 8) release millions of times more
energy than the smallest earthquakes felt by people.
-as a result, they are much rarer:
Richter Magnitude Number per year
<2.5 900,000
8.0 or greater One every 5-10 yrs
Intensity
Before Richter devised the magnitude scale, measures of earthquake strength
focused on the severity of damage caused by the earthquake: what is
now referred to as earthquake intensity.
A numerical scale of earthquake intensity was devised in 1902 by the Italian
scientist Giuseppe Mercalli, based on his observations of earthquakes
affecting populated areas in Italy
-this scale specified the amount of damage to different types of
structures
-a modified version of this scale is now used in the United States
-the Modified Mercalli Intensity Scale.
-intensities are designated with Roman numerals, from I to XII.
Intensity is not a precisely measured quantity: its determination is subjective,
-requires assessment of damage to buildings, bridges, roads, hillsides,
and anything else that has been altered by the earthquake.
After intensity values are assigned for many localities surrounding an
earthquake epicenter, they are plotted on a map
-contour lines of equal intensity are drawn to divide the map into
approximate intensity zones.
-producing a seismic intensity map
-example: 1969 Santa Rosa earthquake.
Although seismic intensity maps are not very precise, they can show:
-the approximate location of the epicenter
-the extent of the damaged region
-and the effects of local geology on earthquake damage: damage can
be locally increased by the effects of weak, water-logged soils that
can liquefy during the earthquake (as in the Marina District of S.F.
during the 1989 Loma Prieta earthquake.
INTRODUCTION TO EARTHQUAKE PREDICTION
Great efforts have been directed over the last several decades toward
developing ways to predict future earthquakes
-major research is underway in the U.S., Japan, China, and Russia.
At present we are able to make only very long-term predictions of the
locations of future large earthquakes over the next several decades; these
have several benefits:
-we can strengthen existing structures in the areas at risk
-create zoning laws to prevent construction along active faults
-and prepare disaster plans and educate the public
-these efforts are already well underway in California.
A short-term prediction of an impending quake would be even more
beneficial
-would not prevent the quake, but it would allow us to take measures
to lessen the danger to people:
-could mobilize disaster relief operations
-evacuate structures known to be weak
-shut down hazardous facilities such as nuclear power plants an oil and
gas pipelines.
Experts in the field agree that a useful short-term earthquake prediction
should include several elements:
1) the expected time of the quake to within a few days or weeks
2) the location of the epicenter
3) the approximate magnitude
Unfortuately, we also have to face the fact that a prediction made months or
a year in advance could have serious negative consequences if it turned
out to be incorrect:
-decline in property values
-decline in property tax revenues
-decreased availability of insurance and mortgages
-decline in business activity and investment; job loss
Both the scientific and the social aspects of the earthquake prediction
problem are problematic.
In the mid-1970s there was considerable optimism about the prospects for
short-term earthquake prediction
-to quote from a 1975 article by Frank Press:
"Although the number of case histories is still too small to make a
positive statement about the feasibility of earthquake prediction,
most seismologists would agree that predication is an achievable
goal in the not too distant future."
The present view is more pessimistic, summed up by a quote from a 1987
book on earthquakes by Bruce Bolt of U.C. Berkeley:
"The overall effort, though substantial, gives little reason for optimism
that practical prediction schemes will be realized in the near future
in most areas of the world."
We will look at the advances and the remaining problems in earthquake
prediction.
CLUES FROM RECENT & HISTORICAL SEISMICITY
Patterns of recent and historical seismicity provide major clues to the
probable locations of future large earthquakes.
Seismic Gaps
Most major active faults have segments which have not broken in major
earthquakes for decades or centuries
-while large earthquakes have occurred more recently on adjacent
segments
-the locked segments can be called seismic gaps.
If we looked at a longer-term compilation of earthquake locations, we would
see a similar pattern
-few small quakes have occurred along many fault segments since their
last great earthquake.
The absence of small earthquakes along these fault segments should not be
reassuring
-it indicates that no small slips are occurring to relieve strain
-these fault segments are locked: frictional resistance is holding the
two sides of the fault strongly together
-but as the plates move, elastic strain is slowly accumulating in the
rocks adjacent to the fault
These locked segments are capable of staying locked for decades or longer
-can accumulate considerable amounts of elastic strain before
rupturing in a major earthquake
-present the greatest risk of infrequent but very large quakes.
The southern margin of Alaska includes several seismic gaps:
-this is a convergent plate boundary where Pacific Ocean floor is
subducting northward beneath Alaska and the Aleutian islands
-discrete segments of the boundary have ruptured in very large
earthquakes during this century, including the 1964 quake (M=
8.6)
-leaving three gaps where no quakes have occurred this century
Seismic gaps are the most likely locations for the next great earthquakes on
each plate boundary.
-between 1968 and 1980, 10 major earthquakes (M > 7.5) occurred
within seismic gaps that had been previously identified by
seismologists.
Recognizing seismic gaps on active faults helps to predict where we can
expect to experience major earthquakes
-but much more detailed studies are required to try to predict when we
can expect such a quake to occur.
Recurrence Intervals
Some indications of the timing of quakes can be revealed by the past
behavior of faults
-for many faults, there is evidence that earthquakes of similar
magnitude repeatedly break the same segment of the fault, and
produce similar offsets.
-the time between these repeated quakes is called the recurrence
interval.
One of the best examples of such regular behavior is part of the San Andreas
fault near Parkfield in central California
-Parkfield is the southern termination of the "creeping" section of the
fault
-a few miles NW of town, the fault takes a slight bend, which serves to
isolate the Parkfield section from the creeping section.
Earthquakes have occurred on the Parkfield section in 1857, 1881, 1901,
1922, 1934, and 1966
-the average recurrence interval has been about 22 years +-2, with the
1934 quake coming 10 years early.
The 1857 Parkfield quake occurred several hours before the Ft. Tejon quake
-seismologists speculate that the displacement on the Parkfield
segment may have triggered the larger offset on the segment of the
fault to the south, which must have been already strained to the
breaking point.
The last three Parkfield quakes have been recorded by seismic instruments
-all had magnitudes of 5.6, with a M=5.1 foreshock occurring 17
minutes before the main quake.
-each ruptured the same 20-mile segment of the fault, with the rupture
beginning at the north end.
-seismograms of these three earthquakes recorded at distant stations
are nearly identical in character and amplitude, suggesting similar
amount of energy was released.
Based on the average recurrence interval of 22 years, the next Parkfield
quake was expected between 1988 and 1993, and is now overdue
-just as the 1934 quake came early, the expected quake appears to be
late
-even for this most well-behaved of fault segments, earthquakes are
not as predictably periodic as we would like.
Unfortunately, the U.S.G.S. bet heavily on the predicted arrival time
-they hoped to catch an earthquake in action
-installed hundreds of monitoring devices to record changes in the
crust around the fault before and after the earthquake
-hoping to get data that would help define the mechanism of triggering
of the earthquake, and reveal possible precursor phenomena that
might be used to help provide short-term earthquake predictions.
For larger-magnitude earthquakes, the recurrence interval is considerably
longer than 22 years
-may be over 200 years
-too long to accurately determine it with our short recorded history in
California.
However, if we know the amount of offset that occurs in each major quake,
and the long-term rate at which strain accumulates along the fault, we
can calculate the expected average interval between quakes.
For example, assume that we determine the long-term rate of movement on a
fault averages out to 5 cm/year
-but this occurs in abrupt offsets of 5 m (500 cm) during large
earthquakes
-the earthquake offset divided by the long-term rate gives the interval
between earthquakes
-in this case the recurrence interval is 100 years.
This is the time it takes for elastic strain to build up along the locked fault to
the level at which friction along the fault is finally overcome, and fault
slip can occur.
Both the characteristic offsets during major earthquakes and the long-term
strain rate must be determined by painstaking geologic studies of active
faults
-and recent techniques allow direct estimates of recurrence intervals of
major earthquakes.
-these studies of ancient earthquake effects are sometimes called
paleoseismology.
PALEOSEISMOLOGY
Paleoseismology involves studies of offset landforms such as stream
channels
-and studies of young sediment layers that accumulate in stream
channels, ponds, and marshes along faults.
Stream channels that cross a strike-slip fault like the San Andreas fault have
their downstream portion progressively offset from the upstream portion
-for a while, the stream will flow along the fault, connecting upper and
lower portions
-eventually the distance becomes too great
-a new lower valley is cut straight across the fault, but it will be offset
in turn.
One such offset stream is Wallace Creek, along the San Andreas fault north
of Los Angeles
-the young, active channel has been offset about 130 m by the fault
-an older, abandoned channel is also preserved, offset an even greater
distance.
Studies of the abandoned channel showed that it is filled up by sediment
deposited by a single debris flow
-a flowing mixture of water, mud, and gravel triggered by heavy rains,
that had flowed down the channel and plugged it.
-fragments of fossil wood in the channel fill deposit were dated by the
Carbon-14 technique: 3,700 years old.
This plugging of the old channel was the event that triggered the cutting of
the present downstream channel segment
-this segment therefore began to form 3,700 years ago
-has been offset about 130 m in that time
-dividing the total offset by the time yields a long-term slip rate of 3.4
cm/year for the fault.
The Wallace Creek area is part of the San Andreas fault that was last broken
by the 1857 Ft. Tejon earthquake
-amount of offset in this region was about 9 meters.
-some small streams in the area have several abandoned and offset
downstream channels
-the regular spacing between the offset channels suggests that 9 meters
is the typical offset that occurs during major earthquakes in this
area.
If the 130 meters of offset of Wallace Creek is due to successive 9-m offsets
during large quakes
-this would require about 14 such quakes (130/9)
If the 14 earthquakes occurred at regular intervals during the 3700 years
-the average interval between earthquakes would be 3700/14, or about
265 years.
-since the last major quake was in 1857, the most likely time for the
next great earthquake on this part of the fault would be in 2120.
Other studies of the San Andreas fault have looked in more detail at
sediment layers accumulating in ponds and marshes along the fault
-during the long intervals between earthquakes, sediment gradually
accumulates at the surface, burying the last fault break
-but during the next earthquake, this layer may be broken by the fault
movement
-after the earthquake, sediment will again accumulate to form a new,
younger layer that covers up the break.
Sediment sequences such as this are studied by digging trenches across the
active fault trace
-for the San Andreas fault, the fault motion is dominantly horizontal
-but when the horizontal offset is several meters or more, there is
usually at least a little vertical offset that shows up in the trench
walls.
In looking at such a sequence in a trench wall, we use principles of relative
age dating to determine the sequence of events
-the principle of cross-cutting relationships tells us that the fault is
younger than any layer that it cuts
-the principle of superposition tells us that the overlying, unbroken
layer must be younger than the fault motion.
In ponds and marshes, the sediments often contain fragments of charcoal
form fires, or pieces of wood, leaves, or marsh vegetation
-new laboratory techniques allow even small fragments to be dated
using the Carbon-14 technique
-if many layers can be dated, then the age of each faulting event
(earthquake) can be bracketed by these absolute ages.
One of the first studies of this kind was done at Pallett Creek northeast of
Los Angeles
-the southernmost part of the fault that ruptured in 1857
At Pallett Creek, swamp deposits about 6 meters thick were studied
-contained about 80 recognizable sediment layers, deposited over the
last 2,000 years.
-the sequence showed the evidence of a number of large earthquakes,
whose ages could be determined with a possible error of a few
decades: 1720, 1550, 1350, 1080
-in fact, there was evidence for 12 major quakes in the past 1700 years.
The average recurrence interval for major earthquakes in the Pallett Creek
area was calculated to be about 150 years
-but the interval varied from a high of 300 years to a low of 55 years.
Paleoseismic studies such as this have been undertaken along many parts of
the San Andreas fault system
-mostly sponsored by the U.S.G.S.
-they suggest that most parts of the San Andreas fault system are less
regular than the Parkfield segment
-recurrence intervals are at best only a guide to enable geologists to
focus attention on faults most likely to rupture in the near future.
EARTHQUAKE PRECURSORS
The main hope for development of short-term earthquake predictions in the
1970's lay in studies of various types of physical phenomena that have
been seen to occur in the months or days prior to some major
earthquakes …
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Electromagnetism
w or quality improvement; it was just all part of good nursing care. The goal for quality improvement is to monitor patient outcomes using statistics for comparison to standards of care for different diseases
e a 1 to 2 slide Microsoft PowerPoint presentation on the different models of case management. Include speaker notes... .....Describe three different models of case management.
visual representations of information. They can include numbers
SSAY
ame workbook for all 3 milestones. You do not need to download a new copy for Milestones 2 or 3. When you submit Milestone 3
pages):
Provide a description of an existing intervention in Canada
making the appropriate buying decisions in an ethical and professional manner.
Topic: Purchasing and Technology
You read about blockchain ledger technology. Now do some additional research out on the Internet and share your URL with the rest of the class
be aware of which features their competitors are opting to include so the product development teams can design similar or enhanced features to attract more of the market. The more unique
low (The Top Health Industry Trends to Watch in 2015) to assist you with this discussion.
https://youtu.be/fRym_jyuBc0
Next year the $2.8 trillion U.S. healthcare industry will finally begin to look and feel more like the rest of the business wo
evidence-based primary care curriculum. Throughout your nurse practitioner program
Vignette
Understanding Gender Fluidity
Providing Inclusive Quality Care
Affirming Clinical Encounters
Conclusion
References
Nurse Practitioner Knowledge
Mechanics
and word limit is unit as a guide only.
The assessment may be re-attempted on two further occasions (maximum three attempts in total). All assessments must be resubmitted 3 days within receiving your unsatisfactory grade. You must clearly indicate “Re-su
Trigonometry
Article writing
Other
5. June 29
After the components sending to the manufacturing house
1. In 1972 the Furman v. Georgia case resulted in a decision that would put action into motion. Furman was originally sentenced to death because of a murder he committed in Georgia but the court debated whether or not this was a violation of his 8th amend
One of the first conflicts that would need to be investigated would be whether the human service professional followed the responsibility to client ethical standard. While developing a relationship with client it is important to clarify that if danger or
Ethical behavior is a critical topic in the workplace because the impact of it can make or break a business
No matter which type of health care organization
With a direct sale
During the pandemic
Computers are being used to monitor the spread of outbreaks in different areas of the world and with this record
3. Furman v. Georgia is a U.S Supreme Court case that resolves around the Eighth Amendments ban on cruel and unsual punishment in death penalty cases. The Furman v. Georgia case was based on Furman being convicted of murder in Georgia. Furman was caught i
One major ethical conflict that may arise in my investigation is the Responsibility to Client in both Standard 3 and Standard 4 of the Ethical Standards for Human Service Professionals (2015). Making sure we do not disclose information without consent ev
4. Identify two examples of real world problems that you have observed in your personal
Summary & Evaluation: Reference & 188. Academic Search Ultimate
Ethics
We can mention at least one example of how the violation of ethical standards can be prevented. Many organizations promote ethical self-regulation by creating moral codes to help direct their business activities
*DDB is used for the first three years
For example
The inbound logistics for William Instrument refer to purchase components from various electronic firms. During the purchase process William need to consider the quality and price of the components. In this case
4. A U.S. Supreme Court case known as Furman v. Georgia (1972) is a landmark case that involved Eighth Amendment’s ban of unusual and cruel punishment in death penalty cases (Furman v. Georgia (1972)
With covid coming into place
In my opinion
with
Not necessarily all home buyers are the same! When you choose to work with we buy ugly houses Baltimore & nationwide USA
The ability to view ourselves from an unbiased perspective allows us to critically assess our personal strengths and weaknesses. This is an important step in the process of finding the right resources for our personal learning style. Ego and pride can be
· By Day 1 of this week
While you must form your answers to the questions below from our assigned reading material
CliftonLarsonAllen LLP (2013)
5 The family dynamic is awkward at first since the most outgoing and straight forward person in the family in Linda
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The most important benefit of my statistical analysis would be the accuracy with which I interpret the data. The greatest obstacle
From a similar but larger point of view
4 In order to get the entire family to come back for another session I would suggest coming in on a day the restaurant is not open
When seeking to identify a patient’s health condition
After viewing the you tube videos on prayer
Your paper must be at least two pages in length (not counting the title and reference pages)
The word assimilate is negative to me. I believe everyone should learn about a country that they are going to live in. It doesnt mean that they have to believe that everything in America is better than where they came from. It means that they care enough
Data collection
Single Subject Chris is a social worker in a geriatric case management program located in a midsize Northeastern town. She has an MSW and is part of a team of case managers that likes to continuously improve on its practice. The team is currently using an
I would start off with Linda on repeating her options for the child and going over what she is feeling with each option. I would want to find out what she is afraid of. I would avoid asking her any “why” questions because I want her to be in the here an
Summarize the advantages and disadvantages of using an Internet site as means of collecting data for psychological research (Comp 2.1) 25.0\% Summarization of the advantages and disadvantages of using an Internet site as means of collecting data for psych
Identify the type of research used in a chosen study
Compose a 1
Optics
effect relationship becomes more difficult—as the researcher cannot enact total control of another person even in an experimental environment. Social workers serve clients in highly complex real-world environments. Clients often implement recommended inte
I think knowing more about you will allow you to be able to choose the right resources
Be 4 pages in length
soft MB-920 dumps review and documentation and high-quality listing pdf MB-920 braindumps also recommended and approved by Microsoft experts. The practical test
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One thing you will need to do in college is learn how to find and use references. References support your ideas. College-level work must be supported by research. You are expected to do that for this paper. You will research
Elaborate on any potential confounds or ethical concerns while participating in the psychological study 20.0\% Elaboration on any potential confounds or ethical concerns while participating in the psychological study is missing. Elaboration on any potenti
3 The first thing I would do in the family’s first session is develop a genogram of the family to get an idea of all the individuals who play a major role in Linda’s life. After establishing where each member is in relation to the family
A Health in All Policies approach
Note: The requirements outlined below correspond to the grading criteria in the scoring guide. At a minimum
Chen
Read Connecting Communities and Complexity: A Case Study in Creating the Conditions for Transformational Change
Read Reflections on Cultural Humility
Read A Basic Guide to ABCD Community Organizing
Use the bolded black section and sub-section titles below to organize your paper. For each section
Losinski forwarded the article on a priority basis to Mary Scott
Losinksi wanted details on use of the ED at CGH. He asked the administrative resident