Prompt What is the goal of education How successful is Ameri.docx

Prompt:
What is the goal of education? How successful is America’s
educational system at achieving that goal for all of this nation’s
children? Examine these questions through two in-class texts
and one outside source.
Assignment Requirements:
1. You must have a clearly defined main point (thesis). The
purpose of the paper is not to tell a story. Rather, use the
readings and your analysis to prove a point or argue an idea.
2. For this paper you must examine the ideas of two readings
from this unit and one outside source.
a. In-class readings: The authors all write about the education in
some manner. You will choose two writers who help you
address your thesis.
b. Outside source: A source not discussed in class that portrays
or examines education. Consider consulting:
i. the media (movies, television, advertisements, etc.).
ii. magazines or newspaper articles
iii. appropriate internet sites
iv. journals (available through the library’s website)
3. You must include a minimum of six quotes from your
sources, but make sure these references are relevant to your
essay. Be sure to give distinctive details, descriptions,
explanations, etc.
4. You must write about an issue, an idea, and not primarily
about your personal experiences.
a. You may draw on personal knowledge to exemplify a point—
indeed, that can be wonderful and effective‐‐, but your personal
story should not take up the bulk of your essay.

5. Your paper should be five to eight pages typed, double
spaced, 12 pt. Times New Roman font and have one inch
margins all the way around. Your essay must also have an
original title.
6. You must use MLA format/conventions for in- text citations
and work cited page.
7. All final drafts of essays must be submitted onto turnitin.com
by the due date. A printed copy of the essay must also be given
to the instructor in class on the day due.
IN CLASS READING:
“Still Unequal, Still Separate” by Jonathan Kozol
“Report of the Massachusetts Board of Education” by Horace
Mann
6 Quotations in total.
OUTSIDE SOURCE:
http://www.nytimes.com/roomfordebate/2015/05/04/is-testing-
students-the-answer-to-americas-education-woes
Geology
doi: 10.1130/G31017.1
2010;38;1067-1070Geology
G.C. Koteas, M.L. Williams, S.J. Seaman and G. Dumond
Granite genesis and mafic-felsic magma interaction in the lower
crust

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GEOLOGY, December 2010 1067
INTRODUCTION
The presence and character of continental
crust on Earth is fundamentally linked to the ori-
gin and evolution of felsic igneous rocks. Many
models for the origin of felsic magmas involve
the input of heat from mafi c magmas emplaced
within or beneath the crust (e.g., Huppert and
Sparks, 1988; Annen et al., 2006). Mafi c mag-
mas also play a role at shallower levels, where
mafi c-felsic magmatic interaction can affect the
longevity and composition of felsic magma sys-
tems (e.g., Wiebe, 1996; Harper et al., 2004). The
fact that mafi c and felsic igneous rocks typically
have a signature of contamination even before
emplacement in the upper crust (DePaolo et al.,
1992; Annen et al., 2006) suggests that the shal-
low crustal interaction may be the fi nal stage in
a protracted set of petrogenetic processes. The
Athabasca granulite terrane (AGT), located in
northwestern Saskatchewan, Canada (Figs. 1A
and 1B), is one of Earth’s largest exposures of
intact lower continental crust and provides an

unprecedented example of felsic magma gen-
eration and felsic-mafi c magma hybridization in
the deep crust. Relationships preserved in this
region fi ll the gap between processes that yield
heat and magma from the mantle and processes
that yield bimodal suites in the shallower crust.
The purpose of this paper is to present detailed
fi eld evidence for granitic magma genesis asso-
ciated with mafi c magmatism within the lower
continental crust and to document evidence for
deep crustal mafi c-felsic magma mingling and
mixing. Exposures in the AGT offer a view of
a fundamental mechanism for contamination
of mantle-derived materials (i.e., assimilation
of crustal components via magma mixing) as
well as felsic magma production from melt-
ing of orthogneiss in the deep crust. The region
provides a picture of a heterogeneous, dynamic,
and locally fertile cratonic deep crust. This set-
ting may serve as a basis for new models of
the behavior of the deep continental crust and
provide insight into the petrogenesis of magmas
observed at shallower crustal levels.
BACKGROUND
The AGT is a >20,000 km2 domain of
Archean to Paleoproterozoic mafi c and felsic
granulites and orthogneisses (Fig. 1B) that were
deformed and metamorphosed at ~1.0–1.2 GPa
(~40 km paleodepths) (Mahan and Williams,
Geology, December 2010; v. 38; no. 12; p. 1067–1070; doi:
10.1130/G31017.1; 2 fi gures; Data Repository item 2010294.

© 2010 Geological Society of America. For permission to copy,
contact Copyright Permissions, GSA, or [email protected]
Granite genesis and mafi c-felsic magma interaction in the
lower crust
G.C. Koteas1, M.L. Williams1, S.J. Seaman1, and G. Dumond2
1Department of Geosciences, University of Massachusetts,
Amherst, Massachusetts 01003, USA
2 Department of Earth, Atmospheric, and Planetary Sciences,
Massachusetts Institute of Technology, Cambridge,
Massachusetts
02142, USA
ABSTRACT
Field observations from an exposed section of deep continental
crust, the Athabasca granu-
lite terrane (AGT), Saskatchewan, Canada, provide a view of
granite genesis and a mechanism
for deep-seated contamination of felsic and mafi c magmas. The
1.9 Ga Chipman mafi c dike
swarm was emplaced into the Chipman Tonalite (ca. 3.3 Ga) and
the megacrystic Fehr granite
(ca. 2.6 Ga) at a crustal depth of ~40 km. The Fehr granite
shows evidence for extensive par-
tial melting and generation of granitic leucosome. Mafi c dikes
and granitic leucosome display
magma mingling and mixing textures similar to those widely
described from shallow crustal
exposures. The AGT provides a view of a dynamic,
heterogeneous, and locally fertile deep
crust. Mantle-derived mafi c magma promotes extensive partial
melting of fertile granitoids,
which in turn fi lter and entrap later mafi c dikes and sills. The
result is almost inevitable min-
gling and hybridization (i.e., contamination) of mafi c and felsic
end members. This interaction

of magmas in the deep crustal environment may account for the
isotopic and compositional
signatures of igneous rocks at shallower crustal levels that
typically record contamination of
crustal melts by mantle material and vice versa.
1000 km
Pacific
Ocean
Atlantic
Ocean
N
North
America
CHURCHILL
Province - Rae
CHURCHILL
Province -
Hearne
Tr
an
s-
Hu
ds
on

Or
og
en
S
N
O
W
B
IR
D
S
N
O
W
B
IR
D
T
E
C
T
O
N
IC
Z
O
N

E
T
E
C
T
O
N
IC
Z
O
N
E
Western limit
of exposed
Canadian Shield
GR
sz
L
L
sz
110 W
60 N
Tr
an
s-

Hu
ds
on
Or
og
en
Ta
ltso
n-T
he
lon
Or
og
en
Archean cratonic provinces
Athabasca granulite terrane
Archean greenstone belts
Hearne Domain (undivided)
Ductile and brittle faults
Grease River shear zone (GRsz)
Legs Lake shear zone (LLsz) Proterozoic basins
Focus area for this study

Aeromagnetic highs in
covered basement
200 km
Steinhauer Lake
Cross Lake
No Name Lake
Fehr Lake
Fe
hr
g
ra
ni
te
C
hi
pm
an
to
na
lit
e
Fehr granite (ca. 2.6 Ga)

5 km
Legs Lake
Le
gs
L
ak
e
S
he
ar
Z
on
e
Lake
Athabasca
Ch
ip
m
an
di
ke
sw
ar

m Chipman tonalite (ca. 3.0 Ga)
S2
N
Equal Area Projection
n = 40
S1
B
C
A
D
N
Figure 1. A: Index map showing location of study. B:
Generalized geologic map of Athabasca
Granulite Terrane (AGT, after Gilboy, 1980; Hanmer, 1997;
Mahan et al., 2005). C: Detailed
map focused on easternmost portion of the AGT including the
Fehr granite, Chipman to-
nalite, and NE-SW−striking Chipman. Chipman dikes are
present throughout area shown
in C (modifi ed from Flowers et al., 2008). Color gradient
within Fehr granite is a schematic
depiction of interpreted intensity of partial melting, white
(most-migmatitic) to gray (least-
migmatitic). D: Stereogram of S
1
(crossed dots) and S

2
(black dots) tectonic fabrics within
migmatized Fehr granite. Hybrid fabrics of S
1
and S
2
commonly observed, especially in
areas of abundant migmatite.
1068 GEOLOGY, December 2010
2005; Williams and Hanmer, 2006). This region
is interpreted to represent continental lower
crust during the period 2.6−1.85 Ga (Mahan et
al., 2006b; Flowers et al., 2006a) (Fig. 1B). It
was uplifted and exhumed along the Legs Lake
thrust-sense shear zone (Fig. 1C) (Mahan and
Williams, 2005, Mahan et al., 2006a, 2006b).
The eastern portion of the AGT is dominated
by the Mesoarchean (3.3 Ga) Chipman tonal-
ite batholith (Fig. 1C), a large body of banded
hornblende tonalite with inclusions of anortho-
site, pyroxenite, and a variety of mafi c and fel-
sic granulites. The Fehr granite (ca. 2.6 Ga; W.
Davis, 1997, personal commun.) occurs along
the eastern fl ank of the Chipman tonalite, just
west of the Legs Lake shear zone (Hanmer et
al., 1994; Hanmer, 1997) (Fig. 1C). The Chip-

man tonalite and the Fehr granite were simulta-
neously intruded by the 1.9 Ga Chipman mafi c
dike swarm (Flowers et al., 2006b).
The most pristine exposures of the Fehr gran-
ite are characterized by euhedral to subhedral
K-feldspar megacrysts (up to 8 cm diameter) in
a matrix of quartz + plagioclase (~1 cm diam-
eter) with fi ne-grained biotite and hornblende
(Fig. 2A). Locally, the long axes of megacrysts
are aligned in a relatively isotropic matrix sug-
gesting preservation of a magmatic fl ow fabric.
More commonly, the Fehr granite has a gneissic
texture, and in many areas, a relatively strong
early foliation (S
1
) is warped into open folds
and cut by a moderately- to steeply-dipping,
northeast-striking axial planar foliation (S
2
)
(Figs. 1D, 2C, and 2D). Aplitic granite pods,
dikes, and sills are common in this area.
The Chipman mafi c dike swarm forms a lin-
ear belt several tens of kilometers in width and
extends for hundreds of kilometers to the north
and south (Williams et al., 1995; Flowers et al.,
2006a). Individual Chipman dikes range from
centimeters to tens of meters in width. These
dikes are composed of hornblende + plagio-
clase + clinopyroxene + garnet and locally,

tonalitic leucosome, which is interpreted as
partial melt of Chipman dikes (Williams et al.,
1995). Internal textures vary markedly based
on the amount of tonalitic leucosome present.
Relatively late-stage dikes are straight-sided
and cut all fabrics in the Chipman tonalite
and Fehr granite. Earlier dikes are commonly
folded and locally contain metamorphic garnet
and clinopyroxene in addition to tonalitic leu-
cosome. The Chipman dikes are interpreted to
have been syntectonically emplaced and meta-
morphosed (Williams et al., 1995; Hanmer,
1997). Metamorphic assemblages within these
dikes indicate high pressure (1.0−1.2 GPa)
granulite facies conditions, with calculated
temperatures on the order of 750−850 °C (Wil-
liams et al. 1995; Flowers et al., 2006a). Geo-
chemical and isotopic signatures are most con-
sistent with derivation from a predominantly
depleted lithospheric or asthenospheric mantle
source (Flowers et al., 2006a).
PARTIAL MELTING OF THE FEHR
GRANITE
The Fehr granite is a pink, K-feldspar bearing
megacrystic granite or gneiss. Most exposures
also contain pink, aplitic granite in dikes, veins,
pods, and fi ne stringers (interpreted as granitic
leucosome) (Fig. 2D). With increasing abun-
dance of granitic leucosome, K-feldspar mega-
crysts are smaller, more anhedral, and in some
cases are partially replaced by granitic leuco-
some (Fig. 2B). At its most extreme, the replace-
ment of megacrysts results in outcrop exposures

with what appear to be deformed megacrysts but
are, in fact, granitic leucosome pods within a
fi ne grained granitic matrix. Tonalitic leucosome
veins are also locally present, and are probably
derived from neighboring migmatitic Chipman
mafi c dikes. The much more abundant granitic
leucosome is interpreted to represent in situ par-
tial melting of the Fehr granite itself. This inter-
pretation is supported by major and trace ele-
ment geochemical trends that show a cogenetic
relationship between Fehr granitic leucosome
and the Fehr granite protolith (see Fig. DR1 and
Table DR1 in the GSA Data Repository1).
A
C
B
D
FE
1GSA Data Repository item 2010294, Figure DR1
(four bivariant element plots of the ten major divi-
sions of rock units sampled from the study area) and
Table DR1(complementary whole-rock data set used to
generate the four plots in Fig. DR1), is available online
at www.geosociety.org/pubs/ft2010.htm, or on request
from [email protected] or Documents Secretary,
GSA, P.O. Box 9140, Boulder, CO 80301, USA.
Figure 2. Field photos of Fehr granite and Fehr granite–
Chipman mafi c dike inter action

along eastern edge of Athabasca granulite terrane (AGT). A:
Isotropic megacrystic Fehr
granite preserving only weak deformation and limited in-situ
granitic leucosome. B: Dif-
fuse contact between Fehr granite–related leucosome pod with S
1
fabric. C: “Megacren-
ulation” cleavage in migmatitic Fehr granite. Note the
crenulated S
1
fabric and spaced
granitic leucosome-rich S
2
crenulation cleavage. D: Aplitic leucosome (felsic dike) with
trails projecting in from S
2
fabric domains. E: Leucosome-rich Fehr granite chemically
and mechanically interacting with discontinuous mafi c
Chipman dikes. F: Coarse-
grained, leucosome-rich Fehr migmatite and Chipman dike
termination.
GEOLOGY, December 2010 1069
Compositional and textural gradients from
relatively pristine to highly migmatitic Fehr

granite occur on several scales. Regionally, gra-
nitic leucosome segregations tend to be more
abundant in the central (Steinhauer Lake) areas
of the Fehr granite exposure (Fig. 1C). In the
northernmost and southernmost exposures,
local transitions from pristine granite to mig-
matitic granite occur on scales from meters to
tens of meters. Single outcrops preserve varia-
tion in rock texture from granite dominated by
euhedral single-crystal megacrysts to exposures
with few megacrysts and abundant granitic leu-
cosome pods (Fig. 2B).
Garnet is rare or absent in the northern and
southern exposures of the Fehr granite, but is
locally abundant within the more penetratively
deformed and more migmatitic central part of
the exposure area (Fig. 1C). Outcrops in this
area can have 10%–15% garnet, with crystals up
to several centimeters in diameter. Commonly,
pink granitic leucosome segregations occur
adjacent to garnet crystals in triangular “tails”
extending along the dominant foliation. The
garnet-bearing migmatite is interpreted to be
the result of a peritectic melt reaction in which
garnet is produced during biotite dehydration
melting. Textural evidence for in situ melting in
exposures with no garnet is interpreted to refl ect
a different melt reaction, eutectic melting of
hydrous orthogneiss.
Deformational fabrics in the Fehr granite
vary with the abundance of granitic leucosome.
This leucosome fi rst appears along the north-
west-striking, shallowly dipping S

1
foliation as
tails or as lozenge-shaped segregations. With
increasing abundance, segregations are more
commonly aligned along the upright S
2
foliation,
and typically defi ne steeply-dipping, northeast-
striking axial planar foliations to meter-scale
folds (Fig. 1D). In the highly migmatitic central
region, a distinctive megacrenulation fabric is
common (Figs. 2C and 2D) in which the granitic
leucosome veins defi ne both the sigmoidal S
1
traces and a spaced S
2
cleavage. Whereas crenu-
lation cleavage in schists is typically spaced
on a scale of millimeters, the S
2
spacing in the
migmatized Fehr granite is ~10−20 cm. With
increasing granitic leucosome abundance, the S
2

domains typically host progressively larger and
more continuous aplitic dikes (Fig. 2D). The dif-
ferent fabrics and geometries in the Fehr granite
migmatite are interpreted to refl ect the evolving
rheology of the granite with increasing degrees
of partial melting.
FEHR GRANITE - CHIPMAN DIKE
INTERACTION: MAGMA MINGLING
AND MIXING
The Chipman dike swarm intrudes both the
Chipman tonalite and the Fehr granite, but
the physical character of dikes is signifi cantly
different in the two host rocks. Most tonalite-
hosted dikes have straight, sharp, parallel con-
tacts. All observations support the interpretation
that Chipman mafi c magmas intruded an essen-
tially brittle tonalite host. In contrast, although
contacts between Chipman dikes and the Fehr
granite can be straight and sharp, they are more
commonly curving, irregular, and distinctly non-
parallel on opposite sides of individual dikes.
Larger dikes commonly bifurcate into smaller,
anastomosing dikes that end abruptly as thin fi n-
gers or rounded terminations (Fig. 2E). Where
dikes intrude granitic leucosome segregations
and larger aplitic dikes and veins within the Fehr
granite, dike margins typically have pillow-like
shapes (Fig. 2F). These textures suggest that the
Chipman dikes were emplaced into, and locally
interacted with, partially melted Fehr granite.
Chipman mafi c magma and aplitic Fehr gran-
ite-related leucosome were mutually contami-

nated by mixing and mingling processes. Mega-
crysts from the partially melted Fehr granite are
typically present within Chipman dike margins,
and locally, trains of megacrysts are present
well within the mafi c dikes. Aplitic leucosome
commonly projects into mafi c dikes (Fig. 2E),
becoming progressively more diffuse and dis-
persed along strike, ultimately producing thin,
white, millimeter-scale schlieren in the Chip-
man dikes. Chipman dikes that intrude migma-
titic Fehr granite or aplitic partial melt segrega-
tions locally disaggregate into concentrations of
centimeter- to meter-scale, rounded mafi c accu-
mulations (Fig. 2F). These pillow-like mafi c
pods are preferentially oriented with long-axes
parallel to the major northeast-southwest trend
of the dike swarm and have been recognized in
granitic leucosome segregations some distance
from obvious mafi c dikes, suggesting that con-
taminated granitic leucosome can be transported
well away from sites of mafi c dike interaction.
DISCUSSION
The Athabasca granulite terrane preserves
evidence of high high-pressure–high-temper-
ature (P-T) metamorphism, deformation, and
pluton emplacement at ca. 2.6 Ga (Williams
and Hanmer, 2006; Dumond et al., 2010).
The AGT may have remained at deep crustal
levels or may have experienced minor exhu-
mation, but a very large portion of the terrane
underwent a second period of high P-T (1.0−
1.2 GPa) metamorphism and deformation at
1.9 Ga (Mahan and Williams, 2005; Williams
and Hanmer, 2006; Flowers et al., 2006a). The

Chipman mafi c dike swarm was emplaced dur-
ing the second event into the relatively fertile
2.6 Ga Fehr granite and the adjacent Chip-
man tonalite. Locally high temperatures, due
to the proximity of mafi c dikes and/or addi-
tional mafi c magma at depth, led to extensive
anatexis of the Fehr granite. The abundance of
aplitic veins and dikes suggests that the gra-
nitic magma was mobilized to some degree
(Fig. 2D). As the fraction of partial melt in the
Fehr granite increased, it may have become
increasingly diffi cult for subsequent Chipman
dikes to cross-cut the granite, as indicated by
the abundance of irregular, pillow-like dike
terminations in the Fehr granite migmatite
(Figs. 2E and 2F). Instead, dikes apparently
pooled beneath and within the Fehr granite,
providing additional heat for further melting.
One critical question concerns the source
of water for large degrees of melting in these
deep crustal rocks. Melting can be explained by
two mechanisms. Biotite dehydration melting
is indicated by the abundant garnet + granitic
leucosome textures in the central exposures of
migmatized Fehr granite, east of Steinhauer
Lake (Fig. 1C). However, large exposures of
migmatized Fehr granite do not contain gar-
net or other minerals indicative of dehydration
(peritectic) melting, yet textural evidence sup-
ports in situ melting. Partial melting in these
areas is interpreted to represent eutectic melting
resulting from the infl ux of hydrous fl uids. The
Chipman mafi c dikes contain abundant horn-
blende and are interpreted to have been hydrous

at the time of emplacement (Williams et al.,
1995, Flowers et al., 2006b). Crystallization
and subsequent metamorphism of early Chip-
man dikes, and possibly of a genetically related
mafi c underplate, probably provided additional
fl uids for partial melting reactions. The large
degree of partial melt production can be attrib-
uted to a combination of the fertility of the Fehr
granite, the presence of hydrous phases, intro-
duction of water from migmatized Chipman
dikes, and especially, the very high temperatures
(>800 °C) in the vicinity of the dense Chipman
mafi c dike swarm .
Mid- and shallow-level igneous rocks com-
monly have a signature of contamination (e.g.,
DePaolo et al., 1992; Barnes et al., 2002).
Workers typically call upon assimilation of
deep crust to explain this contamination and
many envision the digestion of blocks of con-
tinental crustal materials. Studies of the Fehr
granite migmatite provide a different model,
one in which felsic magma genesis and con-
tamination are fundamentally linked. High
temperatures (>800 °C) and hydration pro-
duced during emplacement and migmatization
of mantle-derived mafi c dikes can lead to exten-
sive melting of granitoids in the deep crust. The
presence of felsic partial melt during continued
dike intrusion allows mixing and mingling of
felsic and mafi c magmas. We suggest that this
type of mafi c-felsic magma interaction can
provide an effi cient means of contamination
of both felsic and mafi c end members at lower
crustal depths prior to migration of magma to
middle or shallow crustal levels.

1070 GEOLOGY, December 2010
Many workers have suggested that mantle
partial melts pond at the dry, mafi c base of the
crust (Huppert and Sparks, 1988; Annen et al.,
2006, their fi gure 1). Feeder dikes (Petford,
1996; Rushmer and Klepeis, 2003; Brown,
2005) or shear zones (Hollister and Crawford,
1986) have been invoked to convey magmas
to shallower crustal levels where mixing and
differentiation processes have been widely
documented. However, the heterogeneity of
lower crustal exposures in the AGT indicates
that the deep crustal “hot zone” of Annen et al.
(2006) is more complex than a site of intrusion
of partial mantle melts into mafi c crust. Rather,
underplating at the base of the crust provides
a thermal engine such that true granites can
form in close proximity to the mantle, creating
a setting where mingling and contamination
are inevitable. Exposures in the AGT provide a
view of a linked and positively reinforcing sys-
tem involving mafi c injection, partial melting
of granitoids, fi ltering and entrapment of mafi c
magma, and ultimately hybridization of felsic
and mafi c end members.
ACKNOWLEDGMENTS
We gratefully acknowledge Rebecca Flowers’ con-

tribution of fi rst recognizing mingling textures in the
Fehr granite. The work was supported by National
Science Foundation Grant EAR-0911421. We ap-
preciate discussions with Kevin Mahan, Michael Jer-
cinovic, Simon Hanmer, and Julien Allaz. We thank
James McLelland, Sandra Wyld, and two anonymous
reviewers for thoughtful reviews of the manuscript.
REFERENCES CITED
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The genesis of intermediate and silicic magmas
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egi084.
Barnes, C.G., Yoshinobu, A.S., Prestvik, T., Nordgu-
len, Ø., Karlsson, H.R., and Sundvoll, B., 2002,
Mafi c magma intraplating: Anatexis and hy-
bridization in arc crust, Bindal Batholith, Nor-
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doi:10.1093/petrology/43.12.2171.
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liams, M.L., and Williams, I.S., 2008, Stabili-
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from the lower crustal record in the western
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Manuscript received 11 January 2010
Revised manuscript received 15 June 2010
Manuscript accepted 1 July 2010
Printed in USA
Paper Reviews
Reading research papers ("primary articles") is partly a matter
of experience and skill, and partly learning the specific
vocabulary of a field. First of all, DON'T PANIC! If you
approach it step by step, even an impossible-looking paper can
be understood. Don’t assume that you should be able to
understand the paper on just one or two readings. Truly

understanding an article may take many reads.
1.) Skim the article. What is the basic idea in the paper?
You’re not trying to understand it at this stage, but just get the
general gist.
2.) Comprehension and vocabulary. These can be handled
separately (vocab first), but I find it easier to tackle both at the
same time. Look up words and phrases that are unfamiliar in a
geological dictionary. Work slowly, section by section. For
instance:
· In the Introduction, note how the context is set. What larger
question is this a part of? The author should summarize and
comment on previous research, and you should distinguish
between previous research and the actual current study. What is
the hypothesis of the paper and the ways this will be tested?
· In the Methods, try to get a clear picture of what was done at
each step. What was actually measured? You may want to make
an outline and/or sketch of the procedures and instruments.
Keep notes of your questions; some of them may be simply
technical, but others may point to more fundamental
considerations that you will use for reflection and criticism
below.
· In the Results look carefully at the figures and tables, as they
are the heart of most papers. A scientist will often read the
figures and tables before deciding whether it is worthwhile to
read the rest of the article! What does it mean to "understand" a
figure? You understand a figure when you can redraw it and
explain it in plain English words.
· The Discussion contains the conclusions that the author would
like to draw from the data. In some papers, this section has a lot
of interpretation and is very important. In any case, this is
usually where the author reflects on the work and its meaning in
relation to other findings and to the field in general.
3.) Reflection and criticism. After you understand the article
and can summarize it, then you can return to broader questions
and draw your own conclusions. It is very useful to keep track

of your questions as you go along, returning to see whether they
have been answered. Often, the simple questions may contain
the seeds of very deep thoughts about the work.
Assignment:
Answer the following questions for your paper.
Your answers may be in point form, either typed or handwritten
and should be long enough to adequately answer the questions.
Please pay attention to the clarity of your writing as well.
Introduction:
· What is the overall purpose of the research?
· How does the research fit into the context of its field? Is it,
for example, attempting to settle a controversy? show the
validity of a new technique? open up a new field of inquiry?
· Do you agree with the author's rationale for studying the
question in this way?
Methods:
· Were the measurements appropriate for the questions the
researcher was approaching?
· Often, researchers need to use "indicators" because they
cannot measure something directly--for example, using seismic
velocities to indicate composition. Were the measures in this
research clearly related to the variables in which the researchers
(or you) were interested?
Results:
· What is the one major finding?
· Were enough of the data presented so that you feel you can
judge for yourself how the experiment turned out?
· Did you see patterns or trends in the data that the author did
not mention? Were there problems that were not addressed?
Discussion:
· Do you agree with the conclusions drawn from the data?

· Are these conclusions over-generalized or appropriately
careful?
· Are there other factors that could have influenced, or
accounted for, the results?
· What further experiments could you think of to continue the
research or to answer remaining questions?
Grading Rubric:
Assignment questions
Analysis of Document
Identification of Key Issues/Main Points
Communication
Exemplary
Fully answers all questions as they pertain to the document;
shows excellent understanding of paper in general
(6-7)
Offers in-depth analysis and interpretation of the document;
distinguishes between fact and opinion; explores reliability of
author (8-10)
Identifies the key issues and main points included in the
primary source; shows understanding of author's goal(s) (5)
Demonstrates excellence in communicating ideas with few or no
errors (3)
Adequate
Answers all questions, understanding of paper is moderate (4-5)
Offers accurate analysis of the document (5-7)
Identifies most but not all of the key issues and main points in
the primary source (3-4)
Ideas are communicated adequately (2)
Minimal
All questions are not answered completely, shows limited

understanding of document (2-3)
Demonstrates only a minimal understanding of the document (2-
4)
Describes in general terms one issue or concept included in the
primary source (2)
Shows difficulty with communicating some concepts of the
article (1)
Attempted
Partially completed questions, lack of understanding of the
paper (1)
Reiterates one or two facts from the document but does not
offer any analysis or interpretation of the document (1)
Deals only briefly and vaguely with the key issues and main
points in the document (1)
Poorly written with many errors (0)
Comments
Grade: /25
Further comments:

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