NEW GEOCHEMICAL AND GEOCHRONOLOGIC DATA FROM THE NORTHERN
SIERRA NEVADA, CALIFORNIA: CONSTRAINTS ON THE PRECONDITIONS
FOR LITHOSPHERIC FOUNDERING
by
Gabriel L. Rotberg
A Prepublication Manuscript Submitted to the Faculty of the
DEPARTMENT OF GEOSCIENCES
In Partial Fulfillment of the Requirements
for the Degree of
MASTER OF SCIENCE
In the Graduate College
THE UNIVERSITY OF ARIZONA
2008
New Geochemical and Geochronologic Data from the Northern Sierra Nevada,
California: Constraints on the Preconditions for Lithospheric Foundering
G. L. Rotberg
University of Arizona, Tucson, Arizona
Abstract
New U-Pb zircon geochronology and Sr and Nd isotope geochemistry data from
19 plutonic rocks in the Mesozoic batholith of the northern Sierra Nevada are presented.
The age distribution of these samples is similar to those in the southern and central Sierra
Nevada, and correlate well with two known high-flux episodes of magmatism from 166.8
to 145.3 Ma and 125.5 to 90.41 Ma. An eastward migration of magmatism in the younger
of these episodes is determined to be approximately 2.5 km/my (R2=0.3), similar to
values calculated from data in the southern Sierra Nevada and in the Coast Mountain
Batholith. Isotopic data show that these plutonic rocks are derived from primitive mantle
and evolved crustal components, but that they can not be generated from a simple twocomponent mixing model. Isotopic ratios in this part of the range, on average, have much
more primitive values of 87Sr/86SrInitial (0.7025 to 0.7060) and εNd (+5.75 to -5.81) than is
seen in the southern and central parts of the Sierra Nevada, and the dominant factor
controlling variations in the Sr and Nd isotopic ratios across the range is probably the
geochemistry of the metamorphic framework rocks, and not changing melt sources
through time.
1. Introduction
Lithospheric Foundering in the Sierra Nevada
The Sierra Nevada has recently become studied as the archetype of lithospheric
removal in Cordilleran style magmatic arcs, a process which plays an important role in
our understanding of the tectonics and development of continental crust. Despite recent
models supporting lithospheric foundering in the Andes, Himalayas, and the southern
Sierra Nevada (Zandt et al., 2004; Kay and Kay, 1993), the process occurs in the lower
crust and mantle, and does not easily lend itself to direct observation. Seismic studies tell
that the high, eastern side of the Sierra Nevada lacks the thick felsic or intermediate
crustal root that would be expected by models built on isostatic balancing, and is instead
underlain by relatively low density mantle with the characteristics of hot peridotite
(Wernicke et al., 1996). Recently, xenolith studies in the southern and central Sierra
2
Nevada have been used to prove the presence and subsequent Cenozoic removal of
garnet-rich eclogite facies rocks and peridotitic mantle lithosphere under the range, direct
evidence for lithospheric foundering in the region (Ducea, 2002).
The thickness and composition with depth of the arc crust are also of particular
interest. Rocks of calc-alkaline composition can not be directly extracted by partial
melting of the mantle (Wyllie, 1984), and some other method of differentiating the melt
post-extraction must take place. The residual lower crustal material produced by this
second differentiation stage are either restites, left behind by partial melting and
extraction, or cumulates, left behind by fractional crystallization in a deep magma
chamber, or some combination of the two. Either the restites or cumulates produced
through this second stage of fractionation will be the mafic counterpart to the felsic or
intermediate granitoids in the upper crust, and at lower crustal depths of at least 40 km
beneath the Sierra Nevada these residues will be within the eclogitic phase.
The process through which the mantle lithosphere and eclogitic crust in the
southern Sierra Nevada has been foundered is not precisely clear. Geochemical analyses
of xenoliths erupted in the Miocene have no signature of subducted components, and are
evidence that the material was unaltered by oceanic lithosphere (Ducea and Saleeby,
1998; 1996). This makes it unlikely that foundering occurred through any mechanism
that would have produced significant incorporation of slab related materials into the
magmatic arc, such as the breaking of the subducting slab, or heating following the
passage of the Mendocino triple junction through the region. Likewise, xenoliths erupted
since 3 Ma have geochemical signatures that are distinctly different from the products of
earlier magmatism, eliminating the possibility that these are simply reheated older
3
lithosphere (Ducea and Saleeby, 1996). It is possible that foundering occurred through
either delamination or as convective removal of the mantle crust and eclogitic lithosphere,
but present evidence does not allow us to distinguish between these two processes.
This Study
In order to understand the processes that have been involved in the removal of the
lower lithosphere below the Sierra Nevada, it will be useful to know where the
foundering has occurred and what differences, both geochemical and structural, existed
between those regions and others where active foundering did not take place. While a
large amount of data has been collected in the central and southern Sierra Nevada, which
comprise over 90% of the magmatic products in the batholith (Ducea, 2001), the northern
parts of the range have not been studied as thoroughly. The batholith is exposed to depths
of up to 35 km in the south, and as little as 4 km in the north, so constraints on the
geochemistry and structure of the crust below these depths has to come from petrologic
investigation of the surface rocks, xenolith studies, or geophysical studies. Evidence from
previous work has shown that the central and southern Sierra Nevada developed a thick
eclogitic root, which was later lost through some mechanism of foundering (Saleeby et al.,
2003, Saleeby and Foster, 2004). We question whether the same is also true for the
northern Sierra Nevada.
This study presents new U-Pb zircon ages, Nd and Sr isotopic data for 19 plutonic
rocks. These sample locations are in two transects across the northern Sierra Nevada, and
span the extent of late Mesozoic magmatism in the cordilleran arc at approximately
38°35'N and 39°20'N. The goal of this study twofold; first to improve upon the relatively
4
low density of zircon ages and isotopic data for plutonic rocks in the northern Sierra
Nevada relative to the southern and central parts of the range, and second to use this data
to identify variations in lithospheric chemistry through space and time. This will help
constrain the composition, age, and vertical structure of the Mesozoic batholith,
specifically with respect to the question of late Cenozoic lithospheric foundering in the
region.
2. Geologic Setting and Previous Work
Broadly, the geologic history of the Sierra Nevada relevant to this study can be
divided into three distinct periods. First, the Precambrian rifting of the Laurentian craton
and subsequent deposition of miogeoclinal sedimentation through Paleozoic time,
followed by truncation of the craton and associated miogeoclinal sediments, accretion,
initiation and shutoff of arc magmatism during the Mesozoic, and finally Cenozoic
volcanism and the foundering of the lower lithosphere.
Precambrian rifting and Paleozoic miogeoclinal sedimentation
Prior to the onset of accretionary tectonics and continental arc magmatism, the
western margin of what is now the North American plate was the site of Precambrian
rifting of the Laurentian craton (Dickinson, 2003). The evidence for timing of the rifting
varies with location, and may represent multiple rift events separated by 160-170 Ma
(Colpron et al., 2002). The earliest record of rifting comes from north of the trans-Idaho
discontinuity, basaltic rocks in the basal horizon of the miogeoclinal succession have
been dated isotopically at 770-735 Ma (Armstrong et al., 1982; Devlin et al., 1988;
5
Rainbird et al., 1996; Colpron et al., 2002). In addition, many basin subsidence analyses
in both Canada and the USA area present evidence that subsidence and the miogeoclinal
sedimentation that followed did not begin until 560-555 Ma (Bond et al., 1983; Armin &
Mayer, 1983; Bond and Kominz, 1984; Levy & Chrstine-Blick, 1991). The distinction
between one, two, or many rifting events is not as important for this study as its effect on
the structure and geometry of the western margin of the continent. Miogeoclinal
sedimentation continued at the new passive margin until the onset of accretionary
tectonics along the edge of the craton in the Devonian (Dickinson, 2000).
Late Paleozoic to Mesozoic accretion, Mesozoic arc magmatism
Accretion along the rifted continental margin during Antler-Sonoma orogenesis
began in the Late Devonian and continued through the Early Triassic, as the edge of the
Laurentian craton met the subduction zones of the intraocean island arcs to the west. The
material accreted includes terranes of miogeoclinal ocean sediments, intraocean island
arcs, and island arc subduction complexes (Dickinson, 2008). The initiation of subduction
below the continent and arc related magmatism in the Cordilleran were preceded in the
late Paleozoic by oblique stike-slip faulting and truncation of the passive cratonic edge
and associated miogeoclinal sediments (Hamilton, 1978; Davis et al., 1978). Subduction
was initiated at this truncated margin during mid-Early Triassic time (Dickinson, 2000),
and was the site of continued accretion and the initiation of continental arc magmatism
during the Mesozoic. Accretion along the western margin continued through midCretaceous time, both through incremental accretion within the subduction zone complex,
and through the bulk accretion of coherent tectonic blocks. This addition of this material,
6
along with the intraocean basin sediments, grew the margin of the continent outward to
the west, juxtaposing mature, relatively homogenous cratonic rocks and associated
miogioclinal sediments with a more tectonically and geochemically complex arrangement
of less evolved accreted terranes.
Meanwhile, active subduction beneath the continental margin from 220 to 80 Ma
(Everden and Kistler, 1970; Chen and Moore, 1982; Saleeby et al., 1987) resulted in the
extensive plutonism that would form the Sierra Nevada batholith (Coney & Reynolds,
1977; Dickinson, 1981; Saleeby, 2003). The batholith comprises many distinct granitic
bodies that differ in mineral composition and size, from less than 1 km2 to over 100 km2
(Calkins, 1930; Turner, 1894). In total, approximately 0.7 km3 of tonalitic to
granodioritic magma was produced (Ducea, 2001), and the majority of ages measured for
the plutons are between 85 and 125 Ma (Saleeby et a., 1987). In the southern part of the
Sierra Nevada, this material was intruded into the suture zone between the Proterozoic
craton to the east and the accreted Paleozoic terranes to the west (Saleeby, 2003). In the
northern Sierra Nevada, however, the metamorphic framework into which the batholith
was intruded is well west of the Precambrian continental margin, and comprises only
more immature, accreted material. In the southern Sierra Nevada, this heterogeneity in
the country rocks is evident in the composition of the intrusive plutonic rocks, and is
responsible for the gradient across the range from mafic and tonalitic rocks in the west
and predominantly granodioritic rocks in the east (Moore, 1959. Saleeby, 1981; 1990;
Clemens-Knott, 1992). This change in batholith geochemistry is apparent as a depleted
mantle signature in plutons that interacted with the Paleozoic oceanic crust, and as a
continental signature in plutons that interacted with the Proterozoic cratonic material
7
(Kistler and Peterman, 1973; DePaolo, 1981; Saleeby et al., 1987; Chen and Tilton, 1991;
Clemens-Knott et al., 1991; Coleman et al., 1992; Picket and Saleeby, 1994; Sisson et al.,
1996)
Today, the Sierra Nevada batholith and its associated country rocks have been
uplifted and exposed, forming the mountain range known by the same name. The axis of
the range is oriented approximately NNW-SSE. The batholith constitutes a rigid block
with little internal deformation, despite its apparent westward dip. This gives the Sierra
Nevada an east-west topographic asymmetry, with a steeply dipping eastern front
bounded by fault escarpments, and more gently sloping to western front, which is
covered by Great Valley sediments west of the range. Igneous crystallization depths of
the exposed plutonic rocks vary from less than 4 km in the north (Ague, 1997) to 30 km
in the south (Ague and Brimhall, 1988; Saleeby, 1990; Ague, 1997). Batholiths cover
approximately 90% of the range in the south, and approximately 60-70% of the range in
the north. The more shallowly exposed plutons in the north, along with the metamorphic
basement rocks they have been intruded through, are directly overlain by Eocene river
deposits and late Cenozoic volcanic rocks (Unruh, 1991). Arc magmatism along the
continental margin shut off at 80 Ma with the onset of Laramide flat slab subduction.
Cenozoic volcanism and delamination
Mafic to intermediate composition volcanism, in the form of as many as 150
small volume flows, erupted through the central and southern Sierra Nevada during the
Late Cenozoic (Moore and Dodge, 1980). The volcanism took place during three distinct
stages in the Miocene, the Pliocene, and the Quaternary. A number of these young
8
volcanic rocks contain upper mantle and/or lower crustal xenoliths, which have been used
to constrain the depth, composition, and age of the root beneath the central and southern
Sierra Nevada (Ducea and Saleeby, 1996; 1998; Ducea, 2001). Geochemical studies of
this Late Cenozoic volcanism and entrained xenoliths have proven that the Mesozoic
eclogite root below the central Sierra Nevada was likely removed through some
mechanism of foundering (Ducea and Saleeby, 1996; Manley et al., 2000; Farmer et al.,
2002), and xenolith studies have constrained the removal of the eclogitic root between ~8
and 3 Ma.
3. Samples
In order to define regional geochemical trends in the Mesozoic plutonic rocks of
the northern Sierra Nevada with sufficient detail to compare with pre-existing data in the
southern and central parts of the range, sample locations were chosen for this study
across two transects that run approximately perpendicular to the NNW-SSE axis of the
Sierra Nevada. These transects, which parallel major highways through the range, were
selected for their relatively easy access and outstanding exposure (Figure 1). Nineteen
plutonic rocks across both transects were sampled for analysis, varying in composition
from granite to tonalite (Table 1). Systematic collection and laboratory analysis for age
and geochemical data allows us to generate a data set with a great amount of internal
consistency.
Northern Transect
9
The northern transect comprises eleven samples and follows CA-20 east from
Smartville, California to I-80 at the California-Nevada border. Sample G01 is a
granodiorite from the Yuba Rivers Pluton, and was analyzed for 25 individual U-Pb
zircon analyses, Sr isotopes, and Nd isotopes. Sample G02 is a granodiorite from the
Pleasant Valley Pluton, and was analyzed for 41 individual U-Pb zircon analyses, Sr
isotopes, and Nd isotopes. Sample G03 was collected from the granodiorite just south of
Lake Spaulding, and was analyzed for 25 individual U-Pb zircon analyses as well as Nd
isotopes. Sample G04 was collected from the granodiorite just to the east of Lake
Spaulding, and was analyzed for 35 individual U-Pb zircon analyses, Sr isotopes, and Nd
isotopes. Sample G05, a tonalite was collected from an outcrop just off I-80, north of
Flonston and just west of the California-Nevada border, and was analyzed for Sr and Nd
isotopes. Sample G06 was collected from the granodiorite at Donner Lake, and was
analyzed for 25 individual U-Pb zircon analyses as well as Sr and Nd isotopes. Sample
G08 was collected from the Bowman Lake Granite, and was analyzed for 24 individual
U-Pb zircon analyses, Sr isotopes, and Nd isotopes. Sample G09 was collected from the
granodiorite at Donner Pass, and was analyzed for 25 individual U-Pb zircon analyses, Sr
isotopes, and Nd isotopes. Sample G10 was collected from the granodiorite near Soda
Springs, and was analyzed for 30 individual U-Pb zircon analyses, Sr isotopes, and Nd
isotopes. Sample G11 was collected from the granodiorite west of Cascade Lakes, and
was analyzed for 30 individual U-Pb zircon analyses, Sr isotopes, and Nd isotopes.
Sample G12 was collected from the diorite at Emigrant Gap, and was analyzed for Sr and
Nd isotopes.
10
Southern Transect
The southern transect comprises nine samples and follows CA-88 between
Jackson, California in the west and Markleville, California in the east. Sample G14 was
collected from the granodiorite north of West Point, California, and was analyzed for 25
individual U-Pb zircon analyses, Sr isotopes, and Nd isotopes. Sample G16 was collected
from the granodiorite south of West Point, California, and was analyzed for 25 individual
U-Pb zircon analyses, Sr isotopes, and Nd isotopes. Sample G17 was collected from the
granodiorite near Cooks Station, California, and was analyzed for 25 individual U-Pb
zircon analyses as well as Sr and Nd isotopes. Sample G18 was collected from the
tonalite northwest of Bear River Reservoir, and was analyzed for 25 individual U-Pb
zircon analyses as well as Sr and Nd isotopes. Sample G19 was collected from the
granodiorite west of Silver Lake, and was analyzed for 25 individual U-Pb zircon
analyses, Sr and Nd isotopes. Sample G20 was collected from the granodiorite west of
Gaples Lake, and was analyzed for 30 individual U-Pb zircon analyses, as well as Sr and
Nd isotopes. Sample G21 was collected from the granodiorite west of Carson Pass, and
was analyzed for 25 individual U-Pb zircon analyses, Sr isotopes and Nd isotopes.
Samples G22 and G23 were both collected from outcrops of the Freel Peak Granodiorite.
Sample G22 was collected west of Sorensen’s Camp and was analyzed for 30 individual
U-Pb analyses, Sr isotopes and Nd isotopes. Sample G23 was collected east of
Sorensen’s Camp and was analyzed for 25 individual U-Pb analyses, Sr isotopes and Nd
isotopes.
4. Analytical Techniques
11
Strontium and Neodymium Isotopes
The isotopic ratios of 87Sr/86Sr,
143
Nd/144Nd, and the trace element concentrations
of Rb, Sr, Sm, and Nd were measured all nineteen samples in this study by thermal
ionization mass spectrometry on whole rock samples. Rock samples were crushed to
about one third of their grain size. Rock powders were put in large Savillex vials and
dissolved in mixtures of hot concentrated HF-HNO3. The dissolved samples were spiked
with the Caltech Rb, Sr, and mixed Sm-Nd spikes (Wasserburg et al., 1981; Ducea and
Saleeby, 1998) after dissolution. Rb, Sr, and the bulk of the REEs were separated in
cation columns containing AG50W-X4 resin, using 1N to 4N HCl. Separation of Sm and
Nd was achieved in anion columns containing LN Spec resin, using 0.1N to 2.5N HCl.
Rb was loaded onto single Re filaments using silica gel and H3PO4. Sr was loaded onto
single Ta filaments with Ta2O5 powder. Sm and Nd were loaded onto single Re filaments
using platinized carbon, and resin beads, respectively.
Mass spectrometric analyses were carried out at the University of Arizona on an
11
automated VG Sector multicollector instrument fitted with adjustable 10
Ω Faraday
collectors and a Daly photomultiplier (Ducea and Saleeby, 1998). Concentrations of Rb,
Sr, Sm, Nd were determined by isotope dilution, with isotopic compositions determined
on the same spiked runs. An off-line manipulation program was used for isotope dilution
calculations. Typical runs consisted of acquisition of 100 isotopic ratios. The mean result
of ten analyses of the standard NRbAAA performed during the course of this study is:
85
Rb/87Rb = 2.61199±20. Fifteen analyses of standard Sr987 yielded mean ratios of:
87
Sr/86Sr = 0.710285±7 and 84Sr/86Sr = 0.056316±12. The mean results of five analyses of
the standard nSmβ performed during the course of this study are:
148
Sm/147Sm =
12
0.74880±21, and
148
Sm/152Sm = 0.42110±6. Fifteen measurements of the LaJolla Nd
standard were performed during the course of this study. The standard runs yielded the
following isotopic ratios: 142Nd/144Nd = 1.14184±2, 143Nd/144Nd = 511853±2, 145Nd/144Nd
= 0.348390±2, and
150
Nd/144Nd = 0.23638±2. The Sr isotopic ratios of standards and
samples were normalized to
normalized to
146
86
Sr/88Sr = 0.1194, whereas the Nd isotopic ratios were
Nd/144Nd = 0.7219. The estimated analytical ±2σ uncertainties for
samples analyzed in this study are: 87Rb/86Sr = 0.35%, 87Sr/86Sr = 0.0014%,
= 0.4%, and
143
147
Sm/144Nd
Nd/144Nd = 0.0012%. Procedural blanks averaged from five
determinations were: Rb-10 pg, Sr-150 pg, Sm- 2.7 pg, and Nd - 5.5 pg.
U-Pb Zircon Geochronology
U-Pb geochronology of zircons from all 19 samples in this study was conducted
by laser ablation multicollector inductively coupled plasma mass spectrometry (LA-MCICPMS) at the Arizona LaserChron Center. The analyses involve ablation of zircon with
a New Wave/Lambda Physik DUV193 Excimer laser (operating at a wavelength of 193
nm) using a spot diameter of 25 microns. The ablated material is carried with helium gas
into the plasma source of a GV Instruments Isoprobe, which is equipped with a flight
tube of sufficient width that U, Th, and Pb isotopes are measured simultaneously. All
measurements are made in static mode, using Faraday detectors for 238U and 232Th, an
ion-counting channel for 204Pb, and either faraday collectors or ion counting channels
for 208-206Pb. Ion yields are ~1 mv per ppm. Each analysis consists of one 20-second
integration on peaks with the laser off (for backgrounds), 20 one-second integrations with
13
the laser firing, and a 30 second delay to purge the previous sample and prepare for the
next analysis. The ablation pit is ~15 microns in depth.
For each analysis, the errors in determining 206Pb/238U and 206Pb/204Pb result
in a measurement error of ~1% (at 2-sigma level) in the 206Pb/238U age. The errors in
measurement of 206Pb/207Pb and 206Pb/204Pb also result in ~1% (2-sigma) uncertainty
in age for grains that are >1.0 Ga, but are substantially larger for younger grains due to
low intensity of the 207Pb signal. For most analyses, the cross-over in precision of
206Pb/238U and 206Pb/207Pb ages occurs at ~1.0 Ga.
Common Pb correction is accomplished by using the measured 204Pb and
assuming an initial Pb composition from Stacey and Kramers (1975) (with uncertainties
of 1.0 for 206Pb/204Pb and 0.3 for 207Pb/204Pb). Our measurement of 204Pb is
unaffected by the presence of 204Hg because backgrounds are measured on peaks
(thereby subtracting any background 204Hg and 204Pb), and because very little Hg is
present in the argon gas.
Inter-element fractionation of Pb/U is generally ~20%, whereas fractionation of
Pb isotopes is generally <2%. In-run analysis of fragments of a large zircon crystal
(generally every fifth measurement) with known age of 564 ± 4 Ma (2-sigma error) is
used to correct for this fractionation. The uncertainty resulting from the calibration
correction is generally ~1% (2-sigma) for both 206Pb/207Pb and 206Pb/238U ages.
The analytical data are reported in Table 2. Uncertainties shown in these tables
are at the 1-sigma level, and include only measurement errors. The reported ages are
determined from the weighted mean (Ludwig, 2003) of the 206Pb/238U or 206Pb/207Pb
ages of the concordant and overlapping analyses (Figure 2). Analyses that are statistically
14
excluded from the main cluster are shown in blue on these figures. Two uncertainties are
reported on these plots. The smaller uncertainty (labeled “mean”) is based on the scatter
and precision of the set of 206Pb/238U or 206PB/207Pb ages, weighted according to
their measurement errors (shown at 1-sigma). The larger uncertainty (labeled “age”),
which is the reported uncertainty of the age, is determined as the quadratic sum of the
weighted mean error plus the total systematic error for the set of analyses. The systematic
error, which includes contributions from the standard calibration, age of the calibration
standard, composition of common Pb, and U decay constants, is generally ~1-2% (2sigma).
5. Results
U-Pb Zircon Ages
U-Pb zircon analyses have been performed on 17 of the granitoid samples in this
study, and the ages determined from these analyses are presented in Table 3. The MSWD
for some samples was as high as 6.0, but the lack of correlation between age and U
concentration for these samples rules out lead loss as reason for the large spread in ages.
Cores and tips were analyzed individually when possible, and no evidence of inheritance
was observed. The oldest age calculated in this study is 370.4 ± 7.19 Ma, from the
Bowman Lake Granite, and the most recent age is 90.41 ± 2.14 Ma. With the exception
of the Bowman Lake Granite, the ages determined from this study generally fall in to two
clusters of ages, an older group of 7 samples ranging in age from 166.8 to 145.3 Ma and a
younger group of 10 samples ranging in age from 125.5 to 90.41 Ma. These age ranges
15
have a good correlation with the clustering of ages in the much larger dataset for the
southern and central Sierra Nevada, interpreted as two periods of high flux in the
magmatic arc concentrated around 160-150 Ma and 100-85 Ma (Ducea 2001), and with
flux rates calculated for the northern Sierra Nevada (Figure 7, pers. comm, Cecil 2008).
Sr and Nd isotopes
Sr and Nd isotopes have been determined for all 19 granitoid samples, and
isotopic ratios have been corrected to their initial values using U-Pb zircon ages. These
results are reported in Table 4. Three of the analyses have anomalously large Rb/Sr ratios,
evidence of contamination or Sr loss, and resulting in
87
Sr/86SrInitial values as high as
0.741. These anomalous Sr ratios are not considered further in this study. The
87
Sr/86SrInitial ratios for the remaining samples lie in the range of 0.7025 to 0.7060, and
can further divided in to two groups. Three of the samples, all from the western end of
the northern transect, have relatively low
87
Sr/86SrInitial values, with a range of 0.7028 to
0.7034. The rest of the samples have higher 87Sr/86SrInitial values, ranging from 0.7048 to
0.7060.
143
Nd/144NdInitial ratios were also determined on the same samples. These values,
converted to εNd notation, are all in the range of +5.75 to -5.81, with the exception of
sample G06, which was calculated to have a very low εNd of -22.63. The exceptional
departure of εNd for this sample with respect to those from closely related plutons is
evidence that this value reflects contamination of the sample, and not a true measure of
the isotopic ratio of the rock, and this value is not further considered for this study. Of the
remaining analyses, only two samples have an εNd value in the range of 0 to +6, and the
16
rest have lower values of 0 to -6. The two samples with positive εNd, G01 and G02, are
the westernmost samples from the northern transect.
6. Discussion
U-Pb Zircon Geochronology
When these ages are plotted against the distance of the samples from the axis of
the range, trends in the location of magmatism over time for the two periods of high flux
become apparent (Figure 3). The migration of magmatism over time is clear in the
younger, eastern part of the batholith, and is recorded in the younging of plutons from
125.5 Ma in the west to 90 Ma in the east. This trend is broadly consistent with ages from
the southern and central Sierra Nevada (Saleeby et al., 2003), and a regression of these
ages yields a migration rate of 2.5 km/my (R2=0.3). This rate is similar to the 2.7 km/yr
reported rate of migration for magmatism in the 120-80 Ma plutons in the Sierra Nevada
Batholith (Chen and Moore, 1982) and the migration rate of 2.7-2.0 km/my reported for
similar ages in the Coast Mountains Batholith (Gehrels et al., in press). The regression of
age data for the older plutons in this study yields a migration rate of 5.4 km/my (R2=0.3),
but this value may be misleadingly large given the wide spatial distribution of the
relatively few ages used to calculate this trend. It seems more likely that these plutons
were intruded penecontemporaneously without systematic temporal variation.
Sr and Nd Isotope Geochemistry
17
87
Sr/86Sr ratios are higher for samples with an evolved, crustal signature, and
lower for samples with an immature or depleted mantle signature. The reverse is true for
143
Nd/144Nd, with depleted mantle signatures typically higher than evolved crustal
signatures. By plotting the 87Sr/86Sr ratio for each sample against Sr concentration (Figure
4) we can determine evaluate the likelihood these samples are the product of twocomponent mixing. In an ideal mixture of two components having different
ratios, the data should form a hyperbola in the coordinates of
(Figure 4a). This hyperbola becomes a straight line when
87
87
87
Sr/86Sr
Sr/86Sr and Sr ppm
Sr/86Sr is replotted against
1/Sr ppm (Figure 4b). In the case of the Sr isotopes, the data form has enough scatter that
it is not reasonable to plot a mixing line or try to estimate end-member compositions.
143
Similarly, the
Nd/144Nd ratio is plotted against Nd concentration in (Figure 5). Again,
the data appear too scattered to be the product of simple, two-component mixing. This is
likely evidence that the plutons have sampled from regions of differing chemical
composition within the crust, as would be expected given the lateral geochemical
heterogeneity through the accreted terrains that make up the metamorphic framework in
the northern Sierra Nevada.
The data shown in Figure 6 indicate a good negative correlation between
144
Nd/143Nd and
87
Sr/86Sr. These data can not uniquely determine the proportions of
mantle versus crustal material in the plutonic rocks sampled (Miller et al., 1988), but can
help qualitatively to identify the sources that contributed to the chemical heterogeneity
across the batholith. By defining two general end members (M is mantle, C is crustal) we
can broadly qualify the relative characteristics of the melt sources. End member M must
have a low
87
Sr/86Sr ratio of no more than 0.703 and a relatively high
144
Nd/143Nd of
18
0.5132-0.5136. This range correlates well with the accepted values for mid-ocean ridge
basalts (MORB). End member C has an
144
87
Sr/86Sr ratio of 0.706 at the minimum, and a
Nd/143Nd no higher than 0.5125. It is likely the isotopic variations in the vertical extent
of the batholith are even larger than those observed in the surficial outcrops, as is the case
in the southern Sierra Nevada (Ducea, 2001). It is worth noting that the crustal
component described in this study has a significantly less evolved isotopic signature than
has been determined as the average for the Cordillera as a whole (Ducea and Barton,
2007). This is evidence for either a less evolved “crustal” source or a less significant
amount of crustal material involved in the petrogenesis of these samples. Regional
variations in the country rock of the Sierra Nevada may hold the explanation for this; the
metamorphic framework through which the arc magmatic products intruded is
predominantly accreted terrains in the north, as opposed to the suture between the
continental craton and accreted terrains observed in the south. These accreted terrains
have a less evolved isotopic signature, and this will be reflected in the isotopic signature
of any sample derived from them.
Studies of the growth of the Cordillera have shown that up to 80-90% of the arc
products can be generated over the span of 10-15 m.y. during magmatic flare-up events
(Reymer and Shubert, 1984; Saleeby, 1990; Ducea and Barton, 1997). Several
mechanisms have been discussed in the literature as possible triggers for flare-up events,
and can be broadly classified as lithospheric extension or delamination (Lee et al., 2006)
or intra-crustal or lithospheric shortening (Ducea, 2001). In the Cordillera, all flare-up
events are correlated with significant negative excursions in the εNd during that time
period (Ducea and Barton, 2007). This divergence of εNd from MORB signatures is
19
interpreted to be an increase in more evolved crustal components to the source of melt
generation, and is interpreted by Ducea (2001) as evidence for shortening as a driving
factor of magmatic flare-up events. The samples analyzed in this study, on the other hand,
don’t appear to show much correlation between episodes of high magmatic flux and
variations in isotopic signature (Figure 7), and it is difficult to say for certain when nearly
all the samples collected have crystallization ages associated with one of these high flux
events. The expected magnitude of any such isotopic excursion might also not be
particularly large, if it follows the pattern seen in the Coast Mountain Batholith (Girardi,
2008) instead of that observed in the central and southern Sierra Nevada (Ducea and
Barton, 2007). The country rock of the northern Sierra Nevada is similar to the CMB in
that the crust is largely accreted oceanic terranes, instead of the relatively high proportion
of evolved, crustal material present in the arc in the central and southern Sierra Nevada.
Alternatively, the variation that is apparent in the data could easily be dominated by the
chemical signature of the framework metamorphic rocks assimilated during petrogenesis,
as opposed to the increased addition of crustal material through shortening and thickening
across the arc. This could be evidence that crustal shortening did not play as large a role
in the orogensis of the northern Sierra Nevada, compared to other parts of the Cordillera,
and the lower flux rates and the lack of correlation between the 144Nd/143Nd and 87Sr/86Sr
with the estimated magmatic flux are a reflection of that.
The spatial variation in the
144
Nd/143Nd and 87Sr/86Sr ratios across the axis of the
range is shown in Figure 8. The isotopic ratios of the samples have a good correlation
with location, with the most primitive isotopic signatures farthest to the west and an
increasingly evolved, crustal signature to the east. This trend is most apparent in the
20
northern transect, which extends farther west relative to the southern transect. I argue that
these spatial variations recorded in the isotopic chemistry of the arc magmatic products
are caused primarily by the geochemical signature of the underlying metamorphic
framework rocks, and are the dominant isotopic signal preserved in the northern part of
the batholith. Unfortunately, without more data constraining the geochemistry of the endmembers that compose either the accreted terrains or the mantle melts, it becomes
difficult to further calculate the composition of the residual material in the lower crust.
6. Conclusions
Sr and Nd isotopic data, as well as U-Pb zircon geochronologic analyses are
presented here for 19 rocks across two transects of the northern Sierra Nevada. These
analyses fill in an area of the Sierra Nevada batholith that has relatively little data. Ages
determined for the samples indicate that magmatism in the northern Sierra Nevada, like
its southern and central counterparts, was dominated by two high-flux magmatic episodes,
from 166.8-145.3 Ma and 125.5-90.41 Ma. The distribution of the older samples, located
on the western side of the range, indicate very little spatial-temporal correlation, whereas
a regression of the ages from 125.5 to 90.41 Ma indicate an eastward migration of
magmatism of approximately 2.5 km/my during that high-flux episode, consistent with
observations from the southern Sierra Nevada (Chen and Moore, 1982) and from the
Coast Mountains Batholith (Gehrels et al., 2008). Sr and Nd isotope ratios measured
across both transects document the variation in the sources of melt generation in the arc,
both spatially and temporally. No strong correlation between Sr and Nd isotopes and the
respective concentrations of these elements is observed, indicating that the petrogenesis
21
of these samples cannot be explained through a simple two-component mixing model. A
strong correlation, however, between Sr and Nd isotope ratios is evidence that the
geochemical signature of these samples is dominated by components of both mantle and
continental material. The isotopic signatures of these granitoid samples is, on average,
significantly less evolved than is seen in the southern and central Sierra Nevada, and
inferred to be the result of crustal assimilation involving a higher component of accreted
oceanic terranes than in the south, which has a substantial component of evolved cratonic
material in the magmatic arc.
A lack of correlation between Sr and Nd isotopes with the timing of high-flux
episodes in the Sierra Nevada can be explained several ways. It indicate that significant
amounts of continental material are not being delivered to the region of melt generation
through shortening, but it is also possible that the less evolved isotopic signature of the
accreted oceanic terrains are simply not producing the large deviations in isotopic
signature seen in southern and central Sierra Nevada (Ducea and Barton, 2007). There is,
on the other hand, a good correlation between isotopic ratios in the plutonic rocks
sampled with the type of metamorphic framework rocks that they are intruded through.
Generally, the samples with the most primitive isotopic signatures are located in the
western metamorphic belt of the northern Sierra Nevada, and the samples with more
evolved isotopic signatures are found farther east.
It is not possible, with this data alone, to tightly constrain the composition or
structure of the lower crust below the northern Sierra Nevada, but they do lend some
insight into the difference in petrologic characteristics of this part batholith with respect
to the southern and central parts of the range. In the northern Sierra Nevada, the more
22
primitive isotopic signature of the metamorphic host rocks appears to be a dominant
factor in the geochemistry of the granitoids intruded through them. This implies
significant differences in the character of these rocks and those in the lower part of the
crust with their counterparts in the central and southern Sierra Nevada, and may prove to
have more similarities petrologically and structurally with those in the Coast Mountains
Batholith.
References
Ague, J.J., 1997, Thermodynamic calculation of emplacement pressures for batholithic rocks, California:
Implications for the aluminum-in-hornblende barometer: Geology, v. 25, p. 563-566.
Ague, J.J., and Brimhall, G.H., 1988, Regional variations in bulk chemistry, mineralogy, and the
compositions of mafic and accessory minerals in the batholiths of California: GSA Bulletin, v. 100, p.
891-910.
Armin, R.A., and Mayer, L., 1983, Subsidence analysis of the Cordilleran miogeocline: implications for
timing of late Proterozoic rifting and amount of extension: Geology, v. 11, p. 702-705.
Armstrong, R.L., Eisbacher, G.H., and Evans, P.D., 1982, Age and stratigraphic-tectonic significance of
Proterozoic diabase sheets, Mackenzie Mountains, northwestern Canada: Can. J. Earth Sci., v. 19, p.
316-325.
Bond, G.C., and Kominz, M., 1984, Construction of tectonic subsidence curves for the early Paleozoic
miogeocline, southern Canadian Rocky Mountains: implications for subsidence mechanisms, age of
breakup, and crustal thinning.: Geol. Soc. Am. Bull., v. 95, p. 155-173.
Bond, G.C., Kominz, M., and Devlin, W.R., 1983, Thermal subsidence and eustasy in the lower Paleozoic
miogeocline of western North America: Nature, v. 306, p. 775-779.
Calkins, F.C., 1930, The granitic rocks of the Yosemite region, in Matthes, F.C., ed., Geologic history of
the Yosemite Valley., US Geol Surv Prof Pap 160.
Cecil, M.R., 2008, Flux rates calculated for the northern Sierra Nevada.
Chen, J.H., and Moore, J.G., 1982, Uranium-lead isotopic ages from the Sierra Nevada batholith, California:
Journal of Geophysical Research, v. 87, p. 4761-4784.
Chen, J.H., and Tilton, G.R., 1991, Applications of lead and strontium isotopic relationships to the
petrogenesis of granitoid rocks, central Sierra Nevada batholith, California: Geol. Soc. Am. Bull., v.
103, p. 439-447.
Clemens-Knott, D., 1992, Geologic and isotopic investigations of the Early Cretaceous Sierra Nevada
batholith, Tulare Co, CA and the Ivrea zone, NW Italian Alps: Examples of interaction between mantle
derived magmas and continental crust: Pasadena, Calif. Inst. of Technol.
Clemens-Knott, D., Saleeby, J.B., and Taylor, H.P.J., 1991, O, Sr and Nd constraints on the evolution of
the Early Cretaceous Sierra Nevada Batholith: Geol. Soc. Am. Abstr. Prog., v. 23, p. 386.
Coleman, D.S., Frost, T.P., and Glazner, A.F., 1992, Evidence from the Lamarck Granodiorite for rapid
Late Cretaceous crust formation in California: Science, v. 258, p. 1026-1924.
Colpron, M., Logan, J.M., and Mortensen, J.K., 2002, U-Pb zircon age constraint for late Neoproterozoic
rifting and initiation of the lower Paleozoic passive margin of western Laurentia: Can. J. Earth Sci., v.
39, p. 133-143.
Coney, P.J., and Reynolds, S.J., 1977, Cordilleran Benioff zones: Nature, v. 270, p. 403-406.
Davis, G.A., Monger, J.W.H., and Burchfiel, B.C., 1978, Mesozoic construction of the Cordilleran
"collage", central British Columbia to central California, in Howell, D.G., and McDougal, K.A., eds.,
Mesozoic paleogeography of the western United States, Volume 2, Los Angeles, Pacific Section,
23
Society of Economic Paleontologists and Mineralogists Pacific Coast Paleogeography Symposium, p.
1-32.
DePaolo, D.J., 1981, A neodymium and strontium isotopic study of the Mesozoic calc-alkaline granitic
batholiths of the Sierra Nevada and Peninsular Ranges, California: J. Geophys. Res., v. 86, p. 1047010488.
DePaolo, D.J., and Farmer, L.G., 1984, Isotopic data bearing on the origin of Mesozoic and Tertiary
granitic rocks in the western United States: Phil. Trans. R. Soc. Lond., v. 310, p. 743-753.
Devlin, W.J., Brueckner, H.K., and Bond, G.C., 1988, New isotopic data and a preliminary age for
volcanics near the base of the Windermere Supergroup, northeastern Washington, U.S.A.: Can. J.
Earth Sci., v. 25, p. 1906-1911.
Dickinson, W.R., 1981, Plate tectonics and the continental margin of Caliornia, in Ernst, W.G., ed., The
geotectonic development of California: Englewood Cliffs, New Jersey, Prentice-Hall, p. 1-28.
—, 2000, Geodynamic interpretation of Paleozoic tectonic trends oriented oblique to the Mesozoic
Klamath-Sierran continental margin in California., in Gehrels, G.E., ed., Paleozoic and Triassic
Paleogeography and Tectonics of Western Nevada and Northern California, Volume 347: Boulder, CO,
Geol. Soc. Am., p. 209-245.
—, 2008, Accretionary Mesozoic-Cenozoic expansion of the Cordilleran continental margin in California
and adjacent Oregon: Geosphere, v. 4, p. 329-353.
Dickinson, W.R., and Lawton, T.F., 2003, Sequenctial intercontinental suturing as the ultimate control for
Pennsylvanian Ancestral Rocky Mountains deformation: Geology, v. 31, p. 609-612.
Ducea, M., 2001, The California Arc: Thick Granitic Batholiths, Eclogitic Residues, Lithospheric-Scale
Thrusting, and Magmatic Flare-Ups: GSA Today, v. 11, p. 4-11.
Ducea, M.N., 2002, Constraints on the bulk composition and root foundering rates of continental arcs: A
California arc perspective: Journal of Geophysical Research, v. 107, p. 2304-2316.
Ducea, M.N., and Barton, M.D., 2007, Igniting flare-up events in Cordilleran arcs: Geology, v. 35, p. 10471050.
Ducea, M.N., Kidder, S., and Zandt, G., 2003, Arc composition at mid-crustal depths: Insights from the
Coast Ridge Belt, Santa Lucia Mountains, California: Geophysical Research Letters, v. 30, p. 17031706.
Ducea, M.N., and Saleeby, J.B., 1996, Buoyancy sources for a large, unrooted mountain range, the Sierra
Nevada, California: Evidence from xenolith thermobarometry: Journal of Geophysical Research, v.
101, p. 8229-8244.
—, 1998, The age and origin of a thick mafic-ultramafic keel from beneath the Sierra Nevada batholith:
Contrib Mineral Petrol, v. 133, p. 169-185.
Everden, J.F., and Kistler, R.W., 1970, Chronology of emplacement of Mesozoic batholithic complexes in
California and western Nevada: US Geol Surv Prof Paper, v. 623, p. 1-42.
Farmer, L.G., Glazner, A.F., and Manley, C.R., 2002, Did lithospheric delamination trigger late Cenozoic
potassic volcanism in the southern Sierra Nevada, California: GSA Bulletin, v. 114, p. 754-768.
Gehrels, G.E., Rusmore, M., Woodsworth, G., Crawford, M., Andronicos, C., Hollister, L., Patchett, M.,
Ducea, M., Butler, R., Klepeis, K., Davidson, C., Friedman, R., Haggart, J., Mahoney, B., Crawford,
W., Pearson, D., and Girardi, J., 2008, U-Th-Pb geochronology of the Coast Mountains Batholith in
north-coastal British Columbia: constraints on age and tectonic evolution: GSA Bulletin.
Girardi, J., Rusmore, M., Woodsworth, G., Pearson, D., and Manthei, C., 2008, Elemental and Isotopic
Evidence for Positive and Negative Feedback Mechanisms Governing Magmatic Flux in the Coast
Mountains Batholith, British Columbia: unpublished, p. 39.
Hamilton, W., 1978, Mesozoic tectonics of the western United States, in Howell, D.G., and McDougal,
K.A., eds., Mesozoic paleogeography of the western United States, Volume 2, Los Angeles, Pacific
Section, Society of Economic Paleontologists and Mineralogists Pacific Coast Paleogeography
Symposium, p. 33-61.
Kay, R.W., and Kay, S.M., 1993, Delamination and delamination magmatism: Tectonophysics, v. 219, p.
177-189.
Kistler, R.W., and Peterman, Z., 1973, Variations in Sr, Rb, K, Na and initial 87Sr/86Sr in Mesozoic
granitic rocks and intruded wall rocks in central California: Geol. Soc. Am. Bull., v. 84, p. 3489-3512.
Lee, C.T., Cheng, X., and Horodyskyj, U.N., 2006, The development and refinement of continental arcs by
primary basaltic magmatism, garnet pyroxenite accumulation, basaltic recharge and delamination:
Inights from the Sierra Nevada, California: Contrib Mineral Petrol, v. 151, p. 222-242.
24
Levy, M., and Christie-Blick, N., 1991, Tectonic subsidence of the early Paleozoic passive continental
margin in eastern California and southern Nevada.: Geol. Soc. Am. Bull., v. 103, p. 1590-1606.
Ludwig, K.R., 2003, Isoplot 3.00: Berkley Geochronology Center, Special Publication 4, p. 70.
Manley, C.R., Glazner, A.F., and Farmer, L.G., 2000, Timing of volcanism in the Sierra Nevada of
California: Evidence for Pliocene delamination of the batholithic root?: Geology, v. 28, p. 811-813.
Miller, C.F., Watson, E.B., and Harrison, T.M., 1988, Perspective on the source, segregation, and transport
of granitoid magmas: Transactions of the Royal Society of Edinburgh: Earth Sciences, v. 79, p. 135156.
Moore, J.G., 1959, The quartz diorite boundary line in the western United Sates: J. Geol., v. 67, p. 197-210.
Moore, J.G., and Dodge, F.C.W., 1980, Late Cenozoic volcanic rocks of the southern Sierra Nevada,
California: I. Petrology and Geology: Geol. Soc. Am. Bull., v. 91, p. 1995-2038.
Pickett, D.A., and Saleeby, J.B., 1994, Nd, Sr, and Pb isotopic characteristics of Cretaceous intrusive rocks
from deep levels of the Sierra Nevada batholith, Tehachapi Mountains, California: Contrib Mineral
Petrol, v. 119, p. 198-205.
Rainbird, R.H., Jefferson, C.W., and Young, G.M., 1996, The early Neoproterozoic sedimentary succession
B of northwestern Laurentia: correlations and paleogeographic significance: Geol. Soc. Am. Bull., v.
108, p. 454-470.
Reymer, A., and Schubert, G., 1984, Phanerozoic addition rates to the continental-crust and crustal growth:
Tectonics, v. 3, p. 63-77.
Saleeby, J., 2003, Segmentation of the Laramide Slab - evidence from the southern Sierra Nevada region:
GSA Bulletin, v. 115, p. 655-668.
Saleeby, J., and Foster, Z., 2004, Topographic response to mantle lithosphere removal in the southern
Sierra Nevada region, California: Geology, v. 32, p. 245-248.
Saleeby, J.B., 1981, Ocean floor accretion and volcanoplutonic arc evolution of the Mesozoic Sierra
Nevada, California, in Ernst, W.G., ed., Rubey Volume of the Geotectonic Development of California:
Old Tappan, New Jersey, Prentice-Hall, p. 132-181.
—, 1990, Progress in tectonic and petrogenetic studies in an exposed cross-section of young (~100 Ma)
continental crust, southern Sierra Nevada, California, in Salisbury, M.H., ed., Exposed Cross Sections
of the Continental Crust: Norwell, Mass., D. Reidel, p. 137-158.
Saleeby, J.B., Sams, D.B., and Kistler, R.W., 1987, U/Pb zircon, strontium, and oxygen isotopic and
geochronological study of the southernmost Sierra Nevada batholith, California.: Journal of
Geophysical Research, v. 92, p. 10443-10466.
Sisson, T.W., Grove, T.L., and Coleman, D.S., 1996, Hornblende gabbro sill complex at Onion Valley,
California, and a mixing origin for the Sierra Nevada batholith: Contrib Mineral Petrol, v. 126, p. 81108.
Stacey, J.S., and Kramers, J.D., 1975, Approximation of terrestrial lead isotope evolution by two-stage
model: Earth and Planetary Science Letters, v. 26, p. 207-221.
Turner, H.W., 1894, Rocks of the Sierra Nevada: Fourteenth Ann Rept US Geol Survey Prof Paper, v. 2, p.
441-495.
Unruh, J., 1991, The uplift of the Sierra Nevada and implications for late Cenozoic epeirogeny in the
western Cordillera: Geol. Soc. Am. Bull., v. 103, p. 1395-1404.
Wasserburg, G.J., Jacobsen, S.B., DePaolo, D.J., McCulloch, M.T., and Wen, T., 1981, Precise
determination of Sm/Nd ratios, Sm and Nd isotopic abundances in standard solutions,: Geochim.
Cosmochim. Acta, v. 45, p. 2311-2323.
Wernicke, B., Clayton, R., Ducea, M., Jones, C.H., Park, S.K., Ruppert, S., Saleeby, J., Snow, J.K., Squires,
L., Fleidner, M., Jiracek, G., Keller, R., Kelmperer, S., Luetgert, J., Malin, P., Miller, K., Mooney, W.,
Oliver, H., and Phinney, R., 1996, Origin of High Mountains in the Continents: The Southern Sierra
Nevada: Science, v. 271, p. 190-193.
Wyllie, P.J., 1984, Constrains imposed by experimental petrology on possible and impossible magma
sources and products: Phil. Trans. R. Soc. Lond., v. A310, p. 439-455.
Zandt, G., 2003, The Southern Sierra Nevada Drip and the Mantle Wind Direction Beneath the
Southwestern United States: International Geology Review, v. 45, p. 213-224.
Zandt, G., Gilbert, H., Owens, T.J., Ducea, M., Saleeby, J., and Jones, C.H., 2004, Active foundering of a
continental arc root beneath the southern Sierra Nevada in California: Nature, v. 431, p. 41-46.
25
Figure 1. Simplified geologic map showing the study area, sample locations, and sample
transects. Sample locations are shown as black triangles, transects are shown with black
rectangles. Mesozoic plutonic rocks are shown in pink.
26
Figure 2. U-Pb zircon best ages plotted for each analyses of each sample. Analyses that
are statistically excluded from the main cluster are shown in blue on these figures.
27
Figure 3. U-Pb zircon age plotted with respect to the distance from the range axis for 19
Mesozoic plutonic rocks in the northern Sierra Nevada. Crosses – northern transect; open
circles – southern transect. Solid line represents regression through younger samples
(R2=0.3). Dashed line represents regression through older samples (R2=0.3).
28
Figure 4. A: Initial 87Sr/86Sr vs. Sr concentration in ppm. Samples extracted from a
two-component mixture should plot along the line of a hyperbola. Crosses – northern
transect; open circles – southern transect.
B: Initial 87Sr/86Sr vs. 1/Sr ppm. A two-component mixing line in these coordinates
should plot along a straight line. Symbols as in Figure 4A.
29
Figure 5. A: Initial 144Nd/143Nd vs. Nd concentration in ppm. Samples extracted from
a two-component mixture should plot along the line of a hyperbola. Crosses – northern
transect; open circles – southern transect.
B: Initial 144Nd/143Nd vs. 1/Nd ppm. A two-component mixing line in these
coordinates should plot along a straight line. Symbols as in Figure 4A.
30
Figure 6. Initial 87Sr/86Sr vs. eNd for northern Sierra Nevada plutonic rocks. Sr and Nd
isotopes have a good negative correlation. Crosses – northern transect; open circles –
southern transect.
31
Figure 7. Initial 87Sr/86Sr and eNd vs Age for northern Sierra Nevada plutonic rocks,
plotted against magmatic flux for the northern Sierra Nevada as calculated by Cecil, 2008.
No notable correlation between Sr & Nd isotopes with flux is apparent. Crosses –
northern transect; open circles – southern transect; gray area – magmatic flux.
32
Figure 8. Initial 87Sr/86Sr and eNd vs distance from range crest for northern Sierra
Nevada plutonic rocks. Isotopic signatures trend toward more primitive in the west and
more evolved in the east. Crosses – northern transect; open circles – southern transect;
gray area.
33
Table 1. Sample locations and rock types
Sample
Lattitude
Longitude Rock Type
Location Description
Deg. N.
Deg. W.
Northern Transect
G01
39.29777 121.0882 granodiorite Yuba River Pluton
G02
39.3307 121.1947 granodiorite Pleasant Valley Pluton
G03
39.3219
120.633 granodiorite Lake Spaulding, south
G04
39.32468 120.5981 granodiorite Lake Spaulding, east
G05
39.44328 120.0112 tonalite
north of Flonston
G06
39.33343 120.2906 granodiorite Donner Lake
G08
39.3782
120.671 granite
Bowman Lake Pluton
G09
39.34357 120.3385 granodiorite Donner Pass
G10
39.32757 120.3901 granodiorite Soda Springs
G11
39.31232 120.4946 granodiorite Cascade Lakes, west
G12
39.30613 120.6328 diorite
Emigrant Gap
Southern Transect
G14
38.37207 120.5542 granodiorite north of West Point
G16
38.43558 120.5509 granodiorite south of West Point
G17
38.54627
120.352 granodiorite Cooks Station, CA
Bear River Reservoir,
G18
38.56097 120.2663 tonalite
northwest
G19
38.64565 120.1343 granodiorite Silver Lake, west
G20
38.70483 120.0899 granodiorite Gaples Lake, west
G21
38.69447 119.9956 granodiorite Carson Pass, west
G22
38.77603 119.8968 granodiorite Freel Peak Granodiorite
G23
38.76478 119.8484 granodiorite Freel Peak Granodiorite
34
Table 2. U-Pb geochronologic analyses.
Isotope ratios
Analysis
U/Th
206Pb*
±
207Pb*
±
206Pb*
±
error
206Pb*
±
207Pb*
±
206Pb*
±
Best
age
±
207Pb*
(%)
235U*
(%)
238U
(%)
corr.
238U*
(Ma)
235U
(Ma)
207Pb*
(Ma)
(Ma)
(Ma)
11.0
96.0
176.7
161.6
1.9
U
206Pb
(ppm)
204Pb
G01-1
152
1614
G01-2
140
944
2.7
G01-3
151
1300
1.9
G01-4
146
1208
2.4
20.3744
G01-5
210
2272
3.1
G01-6
109
1648
3.2
G01-7
92
1106
G01-8
497
G01-9
187
G01-10
188
2.0
Apparent ages (Ma)
20.8618
7.5
0.1678
7.6
0.0254
1.2
0.16
161.6
1.9
157.5
19.7132
6.2
17.9750
14.5
0.1755
6.3
0.0251
0.8
0.13
159.8
1.3
164.2
9.5
228.4
144.2
159.8
1.3
0.1948
14.5
0.0254
0.9
0.06
161.6
1.4
180.7
24.0
437.7
323.2
161.6
1.4
15.6
0.1752
15.7
0.0259
1.5
0.09
164.8
2.4
163.9
23.7
151.7
367.0
164.8
2.4
21.3534
8.2
0.1679
8.2
0.0260
0.5
0.06
165.5
0.8
157.6
12.0
40.6
196.0
165.5
0.8
21.9550
12.0
0.1587
12.4
0.0253
3.0
0.25
160.9
4.8
149.6
17.2
-26.3
292.1
160.9
4.8
2.5
22.1408
10.7
0.1562
11.3
0.0251
3.5
0.31
159.7
5.5
147.4
15.5
-46.7
261.4
159.7
5.5
6288
2.2
20.6752
3.6
0.1664
3.7
0.0249
1.0
0.27
158.9
1.6
156.3
5.4
117.2
84.1
158.9
1.6
804
2.1
19.2628
5.7
0.1817
5.9
0.0254
1.4
0.23
161.6
2.2
169.5
9.2
281.6
131.2
161.6
2.2
1472
2.5
20.3355
9.3
0.1644
9.3
0.0242
0.8
0.08
154.4
1.2
154.5
13.4
156.2
218.0
154.4
1.2
G01-12
89
892
3.3
21.5662
11.4
0.1582
11.7
0.0247
2.9
0.25
157.6
4.5
149.1
16.3
16.8
273.8
157.6
4.5
G01-11
182
2778
3.9
20.0672
6.0
0.1695
6.2
0.0247
1.6
0.26
157.1
2.5
159.0
9.1
187.2
140.0
157.1
2.5
G01-13
377
1500
1.9
15.4023
15.5
0.2331
15.6
0.0260
1.4
0.09
165.7
2.2
212.8
29.9
771.9
328.3
165.7
2.2
G01-14
113
1338
2.5
22.5228
13.8
0.1534
13.8
0.0251
1.0
0.07
159.5
1.6
144.9
18.7
-88.5
339.9
159.5
1.6
G01-15
133
1516
2.5
21.2409
14.2
0.1629
14.3
0.0251
1.5
0.10
159.8
2.3
153.3
20.4
53.2
341.3
159.8
2.3
G01-16
135
1064
2.2
18.9291
9.8
0.1825
10.0
0.0251
2.1
0.21
159.5
3.3
170.2
15.7
321.4
222.2
159.5
3.3
G01-17
93
1230
2.9
23.1988
14.3
0.1480
14.3
0.0249
1.7
0.11
158.6
2.6
140.2
18.8
-161.5
355.9
158.6
2.6
G01-18
161
2032
2.0
18.9376
7.8
0.1903
8.1
0.0261
2.0
0.24
166.3
3.2
176.9
13.1
320.4
178.4
166.3
3.2
G01-19
105
910
2.4
19.1260
10.8
0.1928
10.8
0.0267
1.0
0.09
170.1
1.6
179.0
17.7
297.9
246.2
170.1
1.6
G01-20
207
2836
2.5
20.9509
4.7
0.1654
4.9
0.0251
1.7
0.34
160.0
2.7
155.4
7.1
85.9
110.4
160.0
2.7
G01-21
125
1166
2.7
19.5597
7.1
0.1821
7.2
0.0258
1.2
0.17
164.4
2.0
169.9
11.2
246.5
162.8
164.4
2.0
G01-22
92
1216
3.2
21.9698
11.0
0.1583
11.5
0.0252
3.4
0.29
160.6
5.3
149.2
16.0
-27.9
267.2
160.6
5.3
G01-23
167
1044
2.9
22.1352
9.7
0.1506
10.0
0.0242
2.3
0.23
154.0
3.5
142.5
13.3
-46.1
237.1
154.0
3.5
G01-24
175
2258
3.3
21.1503
8.4
0.1664
8.6
0.0255
1.5
0.18
162.4
2.4
156.3
12.4
63.4
200.8
162.4
2.4
G01-25
112
1462
3.0
21.5301
7.7
0.1663
7.8
0.0260
0.5
0.06
165.3
0.8
156.2
11.2
20.8
186.0
165.3
0.8
35
G02-1
150
774
2.0
21.6270
15.3
0.1709
15.5
0.0268
2.3
0.15
170.5
3.9
160.2
22.9
10.1
370.2
170.5
3.9
G02-2
99
762
1.7
23.6095
15.7
0.1492
15.7
0.0256
1.2
0.08
162.7
2.0
141.2
20.7
-205.4
394.8
162.7
2.0
G02-3
164
1120
1.1
21.1298
5.2
0.1712
5.4
0.0262
1.4
0.26
167.0
2.3
160.5
8.0
65.7
123.1
167.0
2.3
G02-4
163
1294
2.0
22.8737
11.2
0.1510
11.2
0.0250
1.3
0.12
159.5
2.1
142.8
15.0
-126.5
276.1
159.5
2.1
G02-5
133
1090
2.2
22.1109
15.0
0.1575
15.1
0.0253
1.5
0.10
160.8
2.4
148.5
20.9
-43.5
367.2
160.8
2.4
G02-6
162
1226
1.8
21.8035
6.6
0.1560
6.8
0.0247
1.6
0.23
157.1
2.4
147.2
9.3
-9.5
160.4
157.1
2.4
G02-7
88
756
2.2
22.2079
9.7
0.1542
9.8
0.0248
1.2
0.12
158.2
1.8
145.6
13.3
-54.1
237.0
158.2
1.8
G02-8
188
1562
2.8
20.9288
4.5
0.1668
5.3
0.0253
2.8
0.53
161.2
4.5
156.6
7.7
88.4
107.1
161.2
4.5
G02-9
121
960
2.0
22.5284
11.3
0.1521
11.7
0.0249
3.0
0.26
158.3
4.7
143.8
15.6
-89.1
276.8
158.3
4.7
G02-10
127
1018
2.6
21.1452
6.3
0.1680
6.4
0.0258
0.9
0.14
164.0
1.5
157.7
9.3
64.0
149.8
164.0
1.5
G02-11
90
710
2.0
23.4477
14.3
0.1503
14.4
0.0256
1.7
0.12
162.7
2.7
142.1
19.1
-188.1
359.3
162.7
2.7
G02-12
86
630
1.9
24.3739
19.7
0.1453
19.7
0.0257
1.1
0.05
163.5
1.7
137.7
25.4
-285.9
506.3
163.5
1.7
G02-13
85
720
1.9
22.8135
12.6
0.1618
12.8
0.0268
2.0
0.15
170.3
3.3
152.3
18.1
-120.0
312.5
170.3
3.3
G02-15
86
742
1.4
22.2000
10.1
0.1600
10.4
0.0258
2.6
0.25
163.9
4.2
150.7
14.6
-53.2
247.0
163.9
4.2
G02-16
105
694
2.4
22.7283
13.8
0.1509
14.0
0.0249
2.8
0.20
158.3
4.4
142.7
18.7
-110.8
340.0
158.3
4.4
G02-17
88
630
1.4
22.8479
13.0
0.1630
13.0
0.0270
0.9
0.07
171.8
1.5
153.3
18.5
-123.7
322.1
171.8
1.5
G02-18
125
980
2.6
22.2721
11.2
0.1531
11.3
0.0247
1.1
0.09
157.5
1.6
144.7
15.2
-61.1
274.2
157.5
1.6
G02-19
120
966
2.0
23.6384
15.4
0.1427
15.6
0.0245
2.6
0.17
155.8
4.0
135.4
19.8
-208.4
387.2
155.8
4.0
G02-20
78
680
1.6
25.4712
21.8
0.1350
22.0
0.0249
2.5
0.11
158.8
3.9
128.6
26.5
-399.4
574.9
158.8
3.9
G02-21
170
1652
2.4
21.6070
6.6
0.1554
8.4
0.0244
5.2
0.61
155.1
7.9
146.7
11.5
12.3
159.2
155.1
7.9
G02-22
109
890
2.0
22.0491
8.9
0.1571
9.0
0.0251
1.6
0.17
159.9
2.5
148.2
12.4
-36.6
215.4
159.9
2.5
G02-23
191
1224
4.6
21.3265
5.2
0.1625
5.6
0.0251
2.2
0.39
160.0
3.4
152.9
7.9
43.6
123.2
160.0
3.4
G02-24
170
1472
2.9
21.1313
5.6
0.1765
5.7
0.0270
1.1
0.19
172.0
1.8
165.0
8.7
65.5
133.3
172.0
1.8
G02-25
211
1622
3.2
20.7732
4.1
0.1657
4.6
0.0250
1.9
0.42
158.9
3.0
155.7
6.6
106.1
98.1
158.9
3.0
G02-26
223
1690
3.1
20.9656
5.1
0.1676
5.9
0.0255
2.9
0.50
162.3
4.7
157.4
8.6
84.2
120.5
162.3
4.7
G02-27
90
844
2.5
26.5036
25.0
0.1297
25.2
0.0249
3.0
0.12
158.7
4.8
123.8
29.4
-504.1
675.1
158.7
4.8
G02-28
134
1092
1.5
21.8198
9.3
0.1522
10.9
0.0241
5.6
0.51
153.5
8.5
143.9
14.6
-11.3
226.3
153.5
8.5
G02-29
132
996
2.6
22.7794
11.7
0.1509
11.9
0.0249
2.0
0.17
158.7
3.1
142.7
15.8
-116.3
289.3
158.7
3.1
G02-30
102
812
2.4
22.0114
9.3
0.1594
9.4
0.0255
1.6
0.17
162.0
2.6
150.2
13.1
-32.5
224.9
162.0
2.6
G02-31
85
586
1.7
22.4798
11.1
0.1557
11.3
0.0254
1.8
0.16
161.6
2.9
146.9
15.4
-83.8
272.9
161.6
2.9
G02-32
325
2332
10.5
21.0234
4.0
0.1563
4.5
0.0238
2.1
0.47
151.9
3.2
147.5
6.2
77.7
94.0
151.9
3.2
G02-33
205
1442
1.4
21.8890
7.6
0.1623
7.6
0.0258
0.5
0.07
164.0
0.8
152.7
10.8
-18.9
184.4
164.0
0.8
36
G02-34
63
576
2.5
24.2674
19.8
0.1490
20.3
0.0262
4.3
0.21
166.9
7.1
141.1
26.7
-274.7
507.5
166.9
7.1
G02-35
1352
6412
15.9
20.1803
1.1
0.1741
1.5
0.0255
0.9
0.63
162.2
1.5
163.0
2.2
174.1
26.3
162.2
1.5
G02-40
128
1166
1.7
21.4468
8.0
0.1662
8.2
0.0258
2.1
0.25
164.5
3.4
156.1
11.9
30.1
191.1
164.5
3.4
G02-41
208
1518
2.5
21.4458
7.4
0.1614
7.6
0.0251
1.7
0.23
159.8
2.7
151.9
10.7
30.3
176.7
159.8
2.7
G03-1
230
3676
2.9
19.7046
5.6
0.1877
5.7
0.0268
1.1
0.20
170.6
1.9
174.7
9.2
229.4
129.6
170.6
1.9
G03-2
228
3872
2.9
20.4348
9.0
0.1701
9.1
0.0252
1.4
0.16
160.5
2.3
159.5
13.5
144.7
212.1
160.5
2.3
G03-4
159
1188
2.9
16.6020
7.0
0.2210
7.0
0.0266
1.0
0.14
169.3
1.7
202.7
13.0
612.0
150.9
169.3
1.7
G03-5
138
1768
2.0
17.7210
8.1
0.2036
8.6
0.0262
2.8
0.33
166.5
4.6
188.1
14.7
469.3
179.5
166.5
4.6
G03-6
102
1496
2.3
18.3815
20.0
0.2005
20.1
0.0267
2.0
0.10
170.1
3.3
185.6
34.1
387.7
452.5
170.1
3.3
G03-7
144
2444
2.7
20.0453
11.3
0.1817
11.3
0.0264
1.0
0.09
168.1
1.7
169.5
17.7
189.7
263.2
168.1
1.7
G03-8
119
2392
2.6
20.0759
14.9
0.1771
15.0
0.0258
1.2
0.08
164.1
1.9
165.6
22.9
186.2
349.6
164.1
1.9
G03-9
125
1948
2.6
17.7707
5.0
0.2055
5.7
0.0265
2.7
0.48
168.6
4.5
189.8
9.9
463.1
111.1
168.6
4.5
G03-10
81
1546
1.6
19.3546
10.0
0.1805
11.8
0.0253
6.2
0.53
161.3
9.9
168.5
18.3
270.7
230.3
161.3
9.9
G03-11
150
2218
2.1
18.5926
9.7
0.1947
9.8
0.0263
2.0
0.20
167.1
3.2
180.6
16.3
362.0
218.1
167.1
3.2
G03-12
132
2314
2.5
19.5248
6.0
0.1829
6.3
0.0259
1.8
0.29
164.8
3.0
170.5
9.9
250.6
138.7
164.8
3.0
G03-13
170
2950
2.6
20.1537
4.4
0.1834
4.9
0.0268
2.1
0.43
170.5
3.5
171.0
7.7
177.1
102.6
170.5
3.5
G03-14
99
1460
2.2
17.1227
16.1
0.2117
16.4
0.0263
2.9
0.18
167.3
4.9
194.9
29.1
544.9
354.2
167.3
4.9
G03-15
104
1904
2.0
22.4700
12.1
0.1586
12.5
0.0258
3.1
0.25
164.5
5.0
149.5
17.3
-82.7
297.1
164.5
5.0
G03-16
206
3228
1.5
18.1628
6.3
0.2019
6.4
0.0266
1.1
0.17
169.2
1.9
186.7
11.0
414.5
142.0
169.2
1.9
G03-19
150
1950
2.3
18.7675
8.1
0.1889
8.3
0.0257
1.8
0.21
163.7
2.8
175.7
13.4
340.9
183.9
163.7
2.8
G03-20
126
2392
1.7
21.3283
11.9
0.1633
12.2
0.0253
2.5
0.20
160.8
3.9
153.6
17.4
43.4
286.2
160.8
3.9
G03-21
94
1646
2.1
19.2398
18.9
0.1820
19.2
0.0254
3.1
0.16
161.7
4.9
169.8
30.0
284.3
435.7
161.7
4.9
G03-22
223
3820
1.7
19.9173
6.6
0.1780
6.9
0.0257
1.9
0.28
163.6
3.1
166.3
10.6
204.6
154.0
163.6
3.1
G03-23
100
1386
2.2
18.7586
6.3
0.1928
6.4
0.0262
1.3
0.19
166.9
2.1
179.0
10.5
341.9
142.9
166.9
2.1
G03-24
113
2080
2.2
17.8457
7.5
0.2004
7.5
0.0259
0.7
0.09
165.1
1.1
185.4
12.8
453.8
166.9
165.1
1.1
G03-25
170
3050
2.8
18.7128
8.3
0.1962
8.8
0.0266
2.8
0.32
169.4
4.6
181.9
14.6
347.5
188.7
169.4
4.6
G04-1
203
2198
1.8
21.4552
6.6
0.1432
6.8
0.0223
1.8
0.26
142.1
2.5
135.9
8.7
29.2
158.4
142.1
2.5
G04-2
62
730
2.2
24.3180
17.4
0.1294
17.8
0.0228
3.9
0.22
145.4
5.6
123.5
20.7
-280.1
445.6
145.4
5.6
G04-3
71
928
1.0
39.8956
50.8
0.0758
50.9
0.0219
2.8
0.05
139.9
3.8
74.2
36.4
######
1891.0
139.9
3.8
G04-4
67
810
1.7
27.0029
25.7
0.1090
25.8
0.0214
2.3
0.09
136.2
3.2
105.1
25.8
-554.1
701.3
136.2
3.2
G04-5
157
1510
0.8
21.6042
11.5
0.1351
12.4
0.0212
4.6
0.37
135.0
6.1
128.7
15.0
12.6
278.2
135.0
6.1
G04-6
61
826
0.8
23.2863
14.5
0.1438
15.2
0.0243
4.5
0.30
154.7
6.9
136.4
19.3
-170.9
361.9
154.7
6.9
37
G04-7
63
604
1.3
23.3168
23.0
0.1322
23.2
0.0224
3.5
0.15
142.6
4.9
126.1
27.6
-174.1
579.4
142.6
4.9
G04-8
149
1382
1.1
22.8002
11.4
0.1298
12.2
0.0215
4.3
0.35
136.9
5.8
123.9
14.2
-118.6
282.3
136.9
5.8
G04-9
139
1274
1.0
21.8086
6.4
0.1336
7.0
0.0211
2.7
0.39
134.8
3.7
127.3
8.3
-10.1
154.9
134.8
3.7
G04-10
92
1042
0.7
22.2170
10.1
0.1257
11.6
0.0202
5.7
0.49
129.2
7.3
120.2
13.1
-55.1
245.3
129.2
7.3
G04-11
306
2252
1.6
21.4390
6.4
0.1454
6.8
0.0226
2.2
0.32
144.1
3.1
137.8
8.8
31.0
154.5
144.1
3.1
G04-12
148
1578
0.8
21.4070
14.8
0.1436
15.0
0.0223
2.2
0.15
142.2
3.1
136.3
19.1
34.6
356.7
142.2
3.1
G04-13
82
824
1.2
23.7036
15.3
0.1267
16.0
0.0218
4.7
0.30
138.9
6.5
121.1
18.3
-215.3
386.3
138.9
6.5
G04-14
55
452
1.1
24.2818
18.6
0.1267
18.8
0.0223
2.9
0.15
142.3
4.0
121.2
21.5
-276.2
476.5
142.3
4.0
G04-15
64
684
1.1
25.6433
23.2
0.1201
23.4
0.0223
3.0
0.13
142.5
4.3
115.2
25.5
-417.0
613.0
142.5
4.3
G04-16
76
978
1.0
23.2121
13.5
0.1305
13.6
0.0220
1.9
0.14
140.1
2.7
124.6
16.0
-162.9
336.5
140.1
2.7
G04-17
197
1752
1.1
21.2560
5.8
0.1579
6.6
0.0243
3.1
0.46
155.0
4.7
148.8
9.1
51.5
139.4
155.0
4.7
G04-18
554
4934
1.5
20.2620
13.1
0.1624
13.2
0.0239
1.8
0.13
152.0
2.7
152.8
18.8
164.6
307.6
152.0
2.7
G04-19
55
788
1.1
26.7432
27.7
0.1181
28.0
0.0229
3.8
0.14
146.0
5.5
113.3
30.0
-528.2
753.7
146.0
5.5
G04-20
381
3902
2.0
21.2469
5.1
0.1543
5.4
0.0238
1.8
0.33
151.5
2.6
145.7
7.3
52.5
120.9
151.5
2.6
G04-21
85
640
0.8
24.9925
19.1
0.1240
19.2
0.0225
1.5
0.08
143.3
2.1
118.7
21.5
-350.2
496.8
143.3
2.1
G04-22
94
874
0.7
23.3521
14.1
0.1333
14.2
0.0226
1.4
0.10
143.9
1.9
127.1
16.9
-177.9
353.2
143.9
1.9
G04-23
56
578
1.3
24.6638
19.2
0.1249
19.3
0.0223
1.8
0.09
142.5
2.6
119.5
21.8
-316.1
497.2
142.5
2.6
G04-24
260
2242
1.1
21.2566
5.5
0.1499
5.6
0.0231
1.2
0.21
147.3
1.7
141.8
7.4
51.5
131.2
147.3
1.7
G04-25
96
1030
1.1
24.0795
17.6
0.1334
17.7
0.0233
2.0
0.11
148.5
2.9
127.2
21.2
-255.0
449.6
148.5
2.9
G04-26
82
718
1.1
24.8401
19.8
0.1298
20.0
0.0234
2.3
0.11
149.0
3.4
123.9
23.3
-334.4
514.3
149.0
3.4
G04-27
72
642
1.1
25.3470
21.4
0.1216
21.5
0.0224
2.0
0.09
142.5
2.8
116.5
23.7
-386.7
563.1
142.5
2.8
G04-28
304
3034
0.6
20.9929
8.8
0.1530
9.0
0.0233
1.9
0.21
148.4
2.8
144.5
12.2
81.2
209.9
148.4
2.8
G04-29
84
526
0.6
24.9308
20.1
0.1226
20.2
0.0222
1.1
0.06
141.3
1.6
117.4
22.4
-343.8
523.7
141.3
1.6
G04-30
77
722
1.1
27.3818
28.5
0.1125
28.6
0.0223
1.9
0.07
142.4
2.7
108.2
29.4
-591.8
787.0
142.4
2.7
G04-31
182
1230
0.4
22.1642
9.1
0.1394
9.3
0.0224
1.8
0.20
142.9
2.6
132.5
11.5
-49.3
222.0
142.9
2.6
G04-32
94
954
1.0
23.1109
12.5
0.1316
12.6
0.0221
2.0
0.16
140.6
2.8
125.5
14.9
-152.1
310.0
140.6
2.8
G04-33
259
1840
1.0
20.9783
5.0
0.1517
5.0
0.0231
0.8
0.15
147.1
1.1
143.4
6.7
82.8
118.1
147.1
1.1
G04-34
308
2526
1.2
21.1168
5.5
0.1545
5.5
0.0237
0.7
0.13
150.7
1.1
145.9
7.5
67.2
130.4
150.7
1.1
G04-35
121
1072
0.8
25.4039
21.4
0.1209
21.6
0.0223
2.4
0.11
142.0
3.4
115.9
23.6
-392.5
563.5
142.0
3.4
G06-1
214
2202
4.0
21.6383
6.2
0.1054
6.5
0.0165
1.8
0.27
105.8
1.9
101.7
6.2
8.8
149.4
105.8
1.9
G06-2
226
1784
3.2
22.2416
7.8
0.1005
7.9
0.0162
1.5
0.19
103.7
1.6
97.3
7.4
-57.8
189.8
103.7
1.6
G06-3
341
2576
3.1
21.3500
4.4
0.1064
4.6
0.0165
1.3
0.29
105.3
1.4
102.6
4.5
41.0
106.1
105.3
1.4
38
G06-4
828
6470
2.2
20.5384
4.7
0.1133
4.9
0.0169
1.5
0.31
107.9
1.6
109.0
5.1
132.9
110.3
107.9
1.6
G06-5
340
2216
2.8
22.1915
8.7
0.1060
9.1
0.0171
2.6
0.29
109.1
2.8
102.3
8.8
-52.3
211.4
109.1
2.8
G06-6
135
1068
2.7
22.7274
10.8
0.1023
10.9
0.0169
1.7
0.16
107.8
1.9
98.9
10.3
-110.7
266.3
107.8
1.9
G06-7
345
2256
2.5
22.0715
6.9
0.1068
6.9
0.0171
0.9
0.14
109.3
1.0
103.0
6.8
-39.1
167.2
109.3
1.0
G06-8
599
4108
1.9
21.3589
3.9
0.1132
4.0
0.0175
0.7
0.18
112.1
0.8
108.9
4.1
40.0
93.4
112.1
0.8
G06-9
543
3534
2.2
21.9510
6.8
0.1118
6.8
0.0178
0.9
0.13
113.8
1.0
107.6
7.0
-25.8
164.0
113.8
1.0
G06-10
286
2182
2.2
21.4201
4.6
0.1120
4.6
0.0174
0.5
0.11
111.2
0.6
107.8
4.7
33.1
110.1
111.2
0.6
G06-11
254
1522
2.5
22.5486
8.9
0.1043
9.2
0.0171
2.4
0.26
109.0
2.6
100.7
8.8
-91.3
218.3
109.0
2.6
G06-12
245
1250
2.6
21.2390
16.2
0.1166
16.2
0.0180
0.5
0.03
114.8
0.6
112.0
17.1
53.4
387.6
114.8
0.6
G06-13
323
2504
2.6
21.7526
5.4
0.1124
5.6
0.0177
1.6
0.28
113.3
1.8
108.1
5.8
-3.9
130.1
113.3
1.8
G06-14
558
4068
3.1
21.4295
3.3
0.1084
3.5
0.0168
1.4
0.39
107.7
1.5
104.5
3.5
32.1
78.1
107.7
1.5
G06-15
500
3576
3.6
20.8982
5.6
0.1114
5.7
0.0169
1.0
0.18
107.9
1.1
107.2
5.8
91.9
131.8
107.9
1.1
G06-16
1020
8128
2.9
20.8815
1.5
0.1138
2.2
0.0172
1.7
0.74
110.2
1.8
109.5
2.3
93.8
36.0
110.2
1.8
G06-17
1469
7164
1.7
20.2743
2.5
0.1117
3.5
0.0164
2.5
0.69
105.0
2.6
107.5
3.6
163.2
59.5
105.0
2.6
G06-18
360
3334
2.8
21.7305
5.0
0.1092
5.5
0.0172
2.3
0.42
110.0
2.5
105.2
5.5
-1.4
119.6
110.0
2.5
G06-19
359
3008
3.3
21.7393
6.0
0.1052
6.1
0.0166
0.8
0.13
106.1
0.9
101.6
5.9
-2.4
145.6
106.1
0.9
G06-20
308
2232
2.4
22.5135
8.7
0.1010
8.7
0.0165
1.0
0.12
105.4
1.1
97.7
8.1
-87.5
213.0
105.4
1.1
G06-21
499
3012
2.4
21.2190
4.4
0.1120
4.7
0.0172
1.7
0.36
110.2
1.8
107.8
4.8
55.7
104.5
110.2
1.8
G06-22
535
3752
1.8
21.1486
4.0
0.1101
4.0
0.0169
0.5
0.13
108.0
0.6
106.1
4.1
63.6
95.0
108.0
0.6
G06-23
419
3100
2.1
21.4414
4.8
0.1094
4.8
0.0170
0.5
0.11
108.7
0.5
105.4
4.8
30.7
114.2
108.7
0.5
G06-24
327
2420
2.5
21.4609
4.6
0.1109
4.6
0.0173
0.7
0.14
110.3
0.7
106.8
4.7
28.6
109.5
110.3
0.7
G06-25
124
980
2.6
23.8889
13.8
0.0943
13.9
0.0163
1.3
0.10
104.5
1.4
91.5
12.1
-234.9
349.8
104.5
1.4
G08-1
260
9894
3.4
18.2184
3.5
0.4572
5.0
0.0604
3.5
0.71
378.1
12.9
382.3
15.9
407.7
79.0
378.1
12.9
G08-2
415
6226
2.4
16.6708
7.0
0.4757
7.2
0.0575
1.8
0.25
360.5
6.2
395.1
23.5
603.0
150.8
360.5
6.2
G08-3
374
11126
2.7
18.1085
1.4
0.4438
2.5
0.0583
2.0
0.81
365.2
7.1
372.9
7.7
421.2
32.2
365.2
7.1
G08-4
299
10438
2.6
18.5794
2.0
0.4236
3.4
0.0571
2.8
0.82
357.8
9.9
358.6
10.4
363.6
44.0
357.8
9.9
G08-5
317
9952
3.3
18.3328
1.7
0.4449
2.8
0.0592
2.2
0.78
370.5
7.9
373.7
8.7
393.7
38.9
370.5
7.9
G08-6
279
7732
2.0
17.7394
2.1
0.4890
2.2
0.0629
0.8
0.37
393.3
3.1
404.3
7.4
467.0
46.0
393.3
3.1
G08-7
330
10916
2.3
18.4609
2.0
0.4556
2.9
0.0610
2.1
0.73
381.7
7.8
381.2
9.1
378.0
44.0
381.7
7.8
G08-8
341
12350
2.0
18.4319
2.2
0.4337
2.7
0.0580
1.6
0.58
363.3
5.6
365.8
8.4
381.6
50.2
363.3
5.6
G08-9
241
8870
3.0
18.4491
3.3
0.4340
3.9
0.0581
2.1
0.53
363.9
7.4
366.0
12.1
379.5
75.1
363.9
7.4
G08-10
402
16862
2.9
17.8769
9.0
0.4761
9.1
0.0617
1.4
0.15
386.1
5.2
395.4
29.7
449.9
199.2
386.1
5.2
39
G08-11
249
7864
3.1
18.4754
3.2
0.4352
3.8
0.0583
2.1
0.54
365.4
7.3
366.9
11.6
376.3
71.0
365.4
7.3
G08-12
284
9696
2.7
18.1045
3.2
0.4572
4.0
0.0600
2.4
0.59
375.8
8.6
382.3
12.7
421.7
72.2
375.8
8.6
G08-13
281
6878
2.9
17.7221
5.7
0.4674
6.1
0.0601
2.3
0.38
376.1
8.4
389.4
19.8
469.2
125.6
376.1
8.4
G08-14
335
2670
2.3
16.4931
11.8
0.4686
11.9
0.0561
1.1
0.09
351.6
3.8
390.2
38.4
626.2
255.2
351.6
3.8
G08-15
442
14702
2.2
18.4378
2.2
0.4358
3.2
0.0583
2.3
0.72
365.1
8.3
367.3
10.0
380.9
50.2
365.1
8.3
G08-16
405
15580
2.1
18.5733
1.7
0.4469
1.8
0.0602
0.7
0.38
376.8
2.5
375.1
5.7
364.4
38.1
376.8
2.5
G08-17
307
7632
2.4
18.3842
5.7
0.4631
5.8
0.0618
1.2
0.21
386.3
4.5
386.4
18.7
387.4
127.9
386.3
4.5
G08-18
445
17018
2.2
18.4895
1.9
0.4406
2.4
0.0591
1.5
0.61
370.1
5.4
370.7
7.6
374.6
43.3
370.1
5.4
G08-19
456
14782
2.1
18.6805
1.6
0.4350
1.7
0.0589
0.7
0.42
369.2
2.7
366.7
5.4
351.4
35.7
369.2
2.7
G08-20
438
12110
1.8
18.3699
2.7
0.4382
3.2
0.0584
1.7
0.54
365.8
6.0
369.0
9.8
389.1
60.2
365.8
6.0
G08-25
251
7760
2.8
17.6402
3.7
0.4510
4.1
0.0577
1.7
0.42
361.7
6.0
378.0
12.8
479.4
81.3
361.7
6.0
G08-21
879
19076
1.6
18.4987
1.3
0.4542
2.8
0.0609
2.5
0.88
381.3
9.2
380.2
8.9
373.4
30.2
381.3
9.2
G08-22
278
11222
2.4
18.2760
2.6
0.4465
3.8
0.0592
2.8
0.73
370.7
10.1
374.9
12.1
400.6
58.9
370.7
10.1
G08-23
311
7230
2.4
18.3443
4.1
0.4494
4.5
0.0598
2.0
0.44
374.4
7.2
376.9
14.2
392.3
91.3
374.4
7.2
G08-24
428
18424
2.1
18.4315
1.8
0.4385
2.5
0.0586
1.8
0.71
367.2
6.4
369.2
7.8
381.6
39.7
367.2
6.4
G09-1
602
6602
2.7
20.5895
4.4
0.1262
4.5
0.0188
1.0
0.22
120.3
1.2
120.6
5.1
127.0
103.4
120.3
1.2
G09-2
464
5164
2.7
21.3359
5.1
0.1201
5.2
0.0186
1.3
0.24
118.7
1.5
115.1
5.7
42.6
121.8
118.7
1.5
G09-3
451
3702
2.2
19.0793
5.8
0.1362
6.1
0.0189
1.8
0.30
120.4
2.2
129.7
7.5
303.4
133.4
120.4
2.2
G09-4
736
5468
2.2
20.1463
4.2
0.1237
4.5
0.0181
1.5
0.33
115.5
1.7
118.4
5.0
178.0
98.8
115.5
1.7
G09-5
509
4458
2.9
19.6220
5.9
0.1316
6.0
0.0187
0.9
0.15
119.6
1.1
125.5
7.1
239.1
136.8
119.6
1.1
G09-6
407
4730
3.4
20.6663
6.9
0.1181
7.0
0.0177
1.3
0.19
113.1
1.5
113.4
7.5
118.3
162.1
113.1
1.5
G09-7
410
5244
3.3
19.7447
6.8
0.1284
6.9
0.0184
1.1
0.15
117.5
1.2
122.7
8.0
224.8
158.2
117.5
1.2
G09-8
469
6120
3.2
20.1151
6.0
0.1229
6.1
0.0179
1.0
0.17
114.6
1.2
117.7
6.8
181.6
140.9
114.6
1.2
G09-9
448
3162
2.8
19.6126
6.0
0.1284
6.2
0.0183
1.5
0.23
116.7
1.7
122.7
7.1
240.2
138.4
116.7
1.7
G09-10
466
5440
2.9
20.2624
4.2
0.1258
4.3
0.0185
0.6
0.14
118.1
0.7
120.3
4.9
164.6
99.3
118.1
0.7
G09-11
555
7034
2.3
20.5526
10.8
0.1242
10.8
0.0185
0.6
0.05
118.3
0.7
118.9
12.2
131.2
255.3
118.3
0.7
G09-12
425
5164
3.4
19.8616
9.4
0.1271
9.5
0.0183
0.8
0.08
117.0
0.9
121.5
10.8
211.1
219.1
117.0
0.9
G09-13
448
6126
2.0
19.0344
3.2
0.1332
3.3
0.0184
0.7
0.21
117.4
0.8
126.9
3.9
308.8
73.0
117.4
0.8
G09-14
546
4962
2.6
18.9681
6.4
0.1305
6.6
0.0180
1.6
0.24
114.7
1.8
124.6
7.7
316.7
144.9
114.7
1.8
G09-15
333
4258
3.5
20.1004
8.8
0.1256
9.1
0.0183
2.4
0.26
117.0
2.7
120.1
10.3
183.3
204.3
117.0
2.7
G09-16
514
7456
3.0
20.4364
3.0
0.1208
3.1
0.0179
0.9
0.29
114.4
1.0
115.8
3.4
144.6
69.7
114.4
1.0
G09-17
554
5928
2.9
19.8964
4.5
0.1239
4.5
0.0179
0.7
0.15
114.3
0.8
118.6
5.1
207.0
104.1
114.3
0.8
40
G09-18
348
4618
3.4
19.5847
6.0
0.1267
6.2
0.0180
1.7
0.28
115.0
2.0
121.2
7.1
243.5
138.1
115.0
2.0
G09-19
602
5308
2.3
19.7180
6.5
0.1247
6.6
0.0178
1.0
0.14
113.9
1.1
119.3
7.4
227.9
150.4
113.9
1.1
G09-20
316
2074
2.9
16.4172
15.3
0.1518
15.3
0.0181
1.6
0.10
115.5
1.8
143.5
20.5
636.1
330.0
115.5
1.8
G09-21
526
5796
2.7
19.9876
4.1
0.1264
4.2
0.0183
0.9
0.20
117.0
1.0
120.8
4.8
196.4
96.3
117.0
1.0
G09-22
781
7360
2.6
20.0045
2.9
0.1227
3.7
0.0178
2.2
0.59
113.7
2.4
117.5
4.1
194.4
68.4
113.7
2.4
G09-23
650
7176
2.0
20.1281
4.5
0.1238
4.5
0.0181
0.7
0.15
115.5
0.8
118.5
5.0
180.1
103.9
115.5
0.8
G09-24
424
5596
3.0
19.8148
7.7
0.1252
7.8
0.0180
1.3
0.17
114.9
1.5
119.7
8.8
216.6
177.5
114.9
1.5
G09-25
585
7278
2.5
20.8811
2.3
0.1182
2.3
0.0179
0.6
0.26
114.4
0.7
113.5
2.5
93.8
53.7
114.4
0.7
G10-1
144
1292
3.3
21.9443
7.4
0.1138
7.4
0.0181
1.0
0.13
115.7
1.1
109.5
7.7
-25.1
178.9
115.7
1.1
G10-2
103
902
3.4
24.2486
17.0
0.1008
17.1
0.0177
1.7
0.10
113.2
1.9
97.5
15.9
-272.7
434.6
113.2
1.9
G10-3
187
1992
3.8
22.7605
11.2
0.1046
11.3
0.0173
1.2
0.10
110.4
1.3
101.0
10.9
-114.3
277.9
110.4
1.3
G10-4
90
1050
3.1
24.4003
16.3
0.0975
16.4
0.0172
1.8
0.11
110.2
1.9
94.4
14.8
-288.7
418.5
110.2
1.9
G10-5
99
800
3.0
24.3352
18.1
0.1032
18.2
0.0182
0.9
0.05
116.4
1.1
99.8
17.3
-281.8
465.3
116.4
1.1
G10-6
169
1612
3.6
23.9716
14.3
0.1076
14.4
0.0187
1.2
0.08
119.4
1.4
103.7
14.2
-243.7
363.7
119.4
1.4
G10-7
356
3124
4.3
21.5275
5.8
0.1147
6.0
0.0179
1.6
0.27
114.4
1.8
110.3
6.3
21.1
139.5
114.4
1.8
G10-8
76
922
3.5
29.1499
31.4
0.0778
31.5
0.0165
3.1
0.10
105.2
3.2
76.1
23.1
-764.7
901.4
105.2
3.2
G10-9
136
1170
3.1
22.9727
10.9
0.1074
10.9
0.0179
1.2
0.11
114.3
1.3
103.6
10.8
-137.2
269.3
114.3
1.3
G10-10
140
1302
3.2
23.0180
11.3
0.1052
11.6
0.0176
2.7
0.23
112.3
3.0
101.6
11.2
-142.1
279.7
112.3
3.0
G10-11
149
1482
3.2
23.8144
14.1
0.1020
14.2
0.0176
1.3
0.09
112.6
1.4
98.7
13.3
-227.1
357.5
112.6
1.4
G10-12
118
1086
3.3
25.5651
20.4
0.0891
20.5
0.0165
2.4
0.12
105.6
2.5
86.7
17.0
-409.0
536.9
105.6
2.5
G10-13
185
1510
3.2
22.5667
8.8
0.1082
8.9
0.0177
1.3
0.15
113.2
1.5
104.4
8.8
-93.2
216.3
113.2
1.5
G10-14
237
2164
3.5
21.7071
6.8
0.1115
7.0
0.0176
1.5
0.21
112.2
1.6
107.3
7.1
1.1
164.7
112.2
1.6
G10-15
240
1888
4.2
21.9314
7.6
0.1053
7.7
0.0167
1.3
0.16
107.1
1.3
101.7
7.5
-23.6
184.5
107.1
1.3
G10-16
147
1234
4.0
23.6009
13.2
0.1008
13.3
0.0172
1.9
0.14
110.2
2.0
97.5
12.4
-204.4
332.4
110.2
2.0
G10-17
157
1382
3.6
23.9759
16.2
0.1006
16.3
0.0175
1.2
0.08
111.8
1.4
97.3
15.1
-244.1
412.4
111.8
1.4
G10-18
178
1772
4.1
22.0503
7.3
0.1052
7.6
0.0168
2.3
0.30
107.5
2.4
101.6
7.4
-36.7
176.7
107.5
2.4
G10-19
316
3366
2.8
21.6965
5.1
0.1099
5.2
0.0173
1.3
0.25
110.5
1.4
105.8
5.3
2.3
122.1
110.5
1.4
G10-20
86
1090
4.9
24.2691
15.2
0.0960
15.3
0.0169
1.5
0.10
108.0
1.6
93.1
13.6
-274.9
389.2
108.0
1.6
G10-21
151
1440
4.4
23.8300
14.9
0.0970
15.1
0.0168
2.2
0.15
107.2
2.4
94.0
13.5
-228.7
377.3
107.2
2.4
G10-22
148
1554
3.8
23.4674
17.4
0.0987
17.5
0.0168
2.3
0.13
107.4
2.4
95.6
16.0
-190.2
437.2
107.4
2.4
G10-23
149
1288
4.4
23.2591
11.5
0.0989
12.3
0.0167
4.4
0.35
106.6
4.6
95.7
11.2
-168.0
287.1
106.6
4.6
G10-24
161
1516
2.5
23.8738
13.8
0.0975
14.0
0.0169
2.7
0.19
108.0
2.9
94.5
12.7
-233.4
348.9
108.0
2.9
41
G10-25
164
1848
5.0
22.4391
16.2
0.1056
16.4
0.0172
2.4
0.14
109.9
2.6
101.9
15.9
-79.4
399.3
109.9
2.6
G10-26
162
1308
2.9
25.0753
19.2
0.0928
19.3
0.0169
1.0
0.05
107.8
1.1
90.1
16.6
-358.7
501.4
107.8
1.1
G10-27
146
1614
3.7
22.1987
16.9
0.1063
16.9
0.0171
1.5
0.09
109.4
1.6
102.6
16.5
-53.1
413.4
109.4
1.6
G10-28
251
1216
3.5
18.8651
12.8
0.1335
12.9
0.0183
1.6
0.12
116.7
1.8
127.2
15.4
329.1
290.8
116.7
1.8
G10-29
267
3280
5.0
20.6066
6.2
0.1200
6.3
0.0179
1.1
0.17
114.6
1.2
115.0
6.9
125.1
146.1
114.6
1.2
G10-30
227
1810
3.3
22.1633
8.0
0.1069
8.1
0.0172
1.4
0.17
109.8
1.5
103.1
8.0
-49.2
195.7
109.8
1.5
G11-1
621
2274
1.4
19.6018
2.4
0.1335
2.7
0.0190
1.4
0.50
121.2
1.6
127.3
3.3
241.5
54.4
121.2
1.6
G11-2
688
4032
2.3
21.2504
3.2
0.1216
3.5
0.0187
1.3
0.38
119.7
1.6
116.5
3.8
52.1
76.5
119.7
1.6
G11-3
478
1442
2.8
19.6173
5.0
0.1325
5.3
0.0189
1.8
0.34
120.4
2.1
126.3
6.3
239.7
115.1
120.4
2.1
G11-4
584
3754
2.9
20.9344
3.4
0.1233
4.1
0.0187
2.3
0.57
119.6
2.7
118.1
4.5
87.8
79.6
119.6
2.7
G11-5
614
2748
2.8
20.9984
3.8
0.1249
4.1
0.0190
1.4
0.34
121.5
1.6
119.5
4.6
80.5
90.8
121.5
1.6
G11-6
720
3896
2.7
20.8491
2.4
0.1217
2.9
0.0184
1.7
0.59
117.5
2.0
116.6
3.2
97.5
55.7
117.5
2.0
G11-7
348
2138
3.1
21.6328
5.4
0.1174
5.6
0.0184
1.7
0.31
117.7
2.0
112.7
6.0
9.4
129.2
117.7
2.0
G11-8
648
3278
2.8
21.3164
3.8
0.1205
4.8
0.0186
2.9
0.61
119.0
3.4
115.5
5.2
44.7
90.4
119.0
3.4
G11-9
600
2856
3.1
21.0941
3.4
0.1233
3.6
0.0189
1.0
0.28
120.5
1.2
118.1
4.0
69.7
81.1
120.5
1.2
G11-10
518
2812
3.2
21.1142
4.1
0.1200
4.8
0.0184
2.4
0.49
117.4
2.7
115.0
5.2
67.5
98.8
117.4
2.7
G11-11
683
2266
2.7
20.3759
3.2
0.1280
3.8
0.0189
2.1
0.54
120.8
2.5
122.3
4.4
151.5
76.1
120.8
2.5
G11-12
487
2268
3.3
19.3831
9.5
0.1313
9.8
0.0185
2.4
0.25
117.9
2.8
125.2
11.5
267.3
218.0
117.9
2.8
G11-13
622
2904
2.2
21.1374
3.9
0.1196
4.2
0.0183
1.7
0.40
117.1
1.9
114.7
4.6
64.9
92.5
117.1
1.9
G11-14
527
2520
2.9
21.5596
4.5
0.1195
5.0
0.0187
2.1
0.43
119.4
2.5
114.6
5.4
17.6
107.6
119.4
2.5
G11-15
684
2388
2.5
20.0962
2.9
0.1306
3.6
0.0190
2.1
0.57
121.6
2.5
124.6
4.2
183.8
68.1
121.6
2.5
G11-16
644
3642
3.0
21.2239
3.9
0.1235
4.2
0.0190
1.7
0.39
121.4
2.0
118.3
4.7
55.1
92.6
121.4
2.0
G11-17
672
2248
2.4
20.1426
4.2
0.1279
4.6
0.0187
1.8
0.40
119.3
2.2
122.2
5.3
178.4
97.9
119.3
2.2
G11-18
499
2284
2.7
20.3561
5.0
0.1305
5.3
0.0193
1.6
0.29
123.0
1.9
124.5
6.2
153.8
118.0
123.0
1.9
G11-19
580
1992
2.7
19.9615
7.5
0.1284
8.0
0.0186
2.8
0.35
118.7
3.2
122.6
9.2
199.4
174.6
118.7
3.2
G11-20
379
950
3.1
14.4271
36.3
0.1758
36.4
0.0184
2.9
0.08
117.5
3.4
164.5
55.4
908.1
773.1
117.5
3.4
G11-21
557
3378
2.6
20.8309
4.3
0.1240
5.0
0.0187
2.5
0.50
119.6
2.9
118.7
5.6
99.5
102.4
119.6
2.9
G11-22
608
3588
2.6
20.8927
4.5
0.1240
5.0
0.0188
2.3
0.46
120.0
2.7
118.7
5.7
92.5
106.5
120.0
2.7
G11-23
460
2090
3.5
20.1190
5.7
0.1273
6.1
0.0186
2.0
0.33
118.6
2.4
121.6
7.0
181.2
134.0
118.6
2.4
G11-24
468
2680
3.0
20.5524
5.0
0.1254
5.8
0.0187
3.0
0.51
119.4
3.5
120.0
6.6
131.3
118.7
119.4
3.5
G11-25
495
2758
3.1
21.3540
4.2
0.1186
5.8
0.0184
3.9
0.68
117.4
4.5
113.8
6.2
40.5
101.6
117.4
4.5
G11-26
820
4158
2.2
20.7155
3.0
0.1270
3.3
0.0191
1.3
0.40
121.9
1.6
121.4
3.7
112.7
70.7
121.9
1.6
42
G11-27
564
2538
2.8
20.2920
3.7
0.1275
4.3
0.0188
2.2
0.51
119.8
2.6
121.8
4.9
161.2
86.5
119.8
2.6
G11-28
620
3040
2.9
20.9598
2.2
0.1251
4.2
0.0190
3.6
0.85
121.4
4.3
119.6
4.7
84.9
52.1
121.4
4.3
G11-29
608
2894
3.0
21.0499
5.6
0.1235
7.0
0.0189
4.2
0.60
120.4
5.1
118.3
7.9
74.7
133.9
120.4
5.1
G11-30
503
1774
3.0
21.0766
3.5
0.1252
4.8
0.0191
3.4
0.70
122.2
4.1
119.8
5.5
71.7
82.6
122.2
4.1
G14-1
447
7912
3.6
20.2877
4.2
0.1774
4.3
0.0261
0.9
0.21
166.1
1.5
165.8
6.6
161.7
99.3
166.1
1.5
G14-2
195
3272
2.5
21.0810
7.9
0.1692
8.0
0.0259
1.1
0.14
164.6
1.8
158.7
11.7
71.2
187.7
164.6
1.8
G14-3
208
3182
2.5
18.4242
10.3
0.1947
10.5
0.0260
1.7
0.16
165.6
2.7
180.6
17.3
382.5
232.9
165.6
2.7
G14-4
394
6610
3.1
19.2413
5.8
0.1840
6.3
0.0257
2.3
0.37
163.4
3.7
171.5
9.9
284.1
133.2
163.4
3.7
G14-5
229
6780
3.7
19.4617
6.6
0.1826
6.7
0.0258
1.4
0.21
164.0
2.3
170.3
10.5
258.0
150.9
164.0
2.3
G14-6
176
1378
2.9
17.4673
10.5
0.2030
10.5
0.0257
1.2
0.11
163.7
1.9
187.7
18.1
501.1
231.2
163.7
1.9
G14-7
878
10556
3.9
18.3901
4.7
0.1916
4.7
0.0256
0.8
0.17
162.7
1.3
178.0
7.7
386.7
104.8
162.7
1.3
G14-8
540
7364
3.3
19.9190
2.9
0.1815
3.1
0.0262
1.0
0.32
166.8
1.6
169.3
4.8
204.4
67.4
166.8
1.6
G14-9
236
4746
1.9
21.7217
7.7
0.1688
7.8
0.0266
1.5
0.19
169.2
2.5
158.4
11.5
-0.4
185.3
169.2
2.5
G14-10
211
2724
1.6
19.8038
12.4
0.1774
12.4
0.0255
0.9
0.07
162.2
1.4
165.8
19.0
217.8
287.5
162.2
1.4
G14-11
104
1672
2.3
20.0968
11.2
0.1745
11.3
0.0254
1.7
0.15
161.9
2.6
163.3
17.1
183.7
261.3
161.9
2.6
G14-12
242
4112
3.1
19.4564
4.7
0.1798
4.9
0.0254
1.2
0.24
161.5
1.9
167.9
7.6
258.7
108.9
161.5
1.9
G14-13
140
2960
3.9
19.1729
8.8
0.1848
9.1
0.0257
2.1
0.23
163.5
3.3
172.2
14.3
292.3
201.9
163.5
3.3
G14-14
244
5556
3.5
18.2513
10.0
0.2010
10.1
0.0266
1.3
0.13
169.3
2.1
186.0
17.2
403.7
225.5
169.3
2.1
G14-15
336
5304
3.0
19.4020
3.7
0.1864
3.9
0.0262
1.0
0.25
166.9
1.6
173.6
6.2
265.1
85.9
166.9
1.6
G14-16
252
4540
3.0
19.5319
6.1
0.1878
6.3
0.0266
1.7
0.27
169.2
2.9
174.7
10.1
249.8
140.0
169.2
2.9
G14-17
277
4934
3.0
18.8408
10.1
0.1930
10.1
0.0264
0.8
0.08
167.8
1.3
179.2
16.6
332.0
229.5
167.8
1.3
G14-18
745
9990
3.9
19.6873
5.4
0.1804
5.5
0.0258
0.9
0.17
164.0
1.5
168.4
8.6
231.5
125.7
164.0
1.5
G14-19
464
10422
4.1
19.6907
3.9
0.1853
4.2
0.0265
1.4
0.33
168.3
2.3
172.6
6.6
231.1
90.9
168.3
2.3
G14-20
189
5534
2.2
22.1127
8.8
0.1609
8.9
0.0258
1.4
0.16
164.2
2.3
151.5
12.5
-43.7
213.9
164.2
2.3
G14-21
312
5954
3.8
20.4422
7.9
0.1807
8.1
0.0268
1.8
0.22
170.4
3.0
168.7
12.5
143.9
184.7
170.4
3.0
G14-22
271
5236
3.8
19.2515
8.5
0.1869
8.6
0.0261
0.8
0.09
166.1
1.2
174.0
13.7
282.9
195.5
166.1
1.2
G14-23
159
3052
3.3
18.4479
11.8
0.1981
11.8
0.0265
0.7
0.06
168.6
1.1
183.5
19.8
379.6
265.2
168.6
1.1
G14-24
432
8360
4.2
19.3206
6.1
0.1831
6.2
0.0257
0.7
0.11
163.3
1.1
170.7
9.7
274.7
140.8
163.3
1.1
G14-25
518
9156
3.3
21.0181
4.7
0.1696
4.9
0.0259
1.4
0.28
164.6
2.2
159.1
7.1
78.3
110.7
164.6
2.2
G16-1
257
3196
3.9
21.1002
5.0
0.1693
5.4
0.0259
2.0
0.37
164.9
3.2
158.8
8.0
69.0
120.0
164.9
3.2
G16-2
602
6204
3.2
20.5360
2.7
0.1764
3.1
0.0263
1.5
0.47
167.2
2.4
165.0
4.7
133.1
64.3
167.2
2.4
G16-3
357
3770
2.2
20.7742
3.0
0.1687
3.7
0.0254
2.2
0.60
161.8
3.6
158.3
5.4
106.0
69.8
161.8
3.6
43
G16-4
324
1598
2.7
18.5035
11.1
0.1932
11.2
0.0259
0.9
0.08
165.0
1.4
179.4
18.4
372.8
251.6
165.0
1.4
G16-5
385
4172
2.6
19.8626
3.7
0.1750
3.9
0.0252
1.3
0.33
160.5
2.1
163.8
5.9
211.0
85.5
160.5
2.1
G16-6
285
3228
3.3
21.1607
6.3
0.1639
6.4
0.0252
1.5
0.24
160.2
2.4
154.1
9.2
62.2
149.3
160.2
2.4
G16-7
427
1528
2.8
17.1566
14.8
0.2072
15.1
0.0258
2.6
0.17
164.1
4.2
191.2
26.3
540.5
326.1
164.1
4.2
G16-8
535
4784
2.1
20.7805
4.1
0.1694
4.2
0.0255
0.6
0.15
162.6
1.0
158.9
6.1
105.3
97.1
162.6
1.0
G16-9
724
10618
3.2
20.6758
2.6
0.1734
2.7
0.0260
0.7
0.26
165.5
1.1
162.4
4.0
117.2
61.2
165.5
1.1
G16-10
701
5596
3.6
20.4915
3.7
0.1673
3.9
0.0249
1.2
0.30
158.3
1.8
157.1
5.6
138.2
86.9
158.3
1.8
G16-11
619
4480
3.7
20.2561
2.1
0.1807
3.0
0.0265
2.2
0.73
168.9
3.6
168.6
4.7
165.3
48.2
168.9
3.6
G16-12
312
3088
2.4
21.3366
5.8
0.1684
6.1
0.0261
2.0
0.33
165.8
3.3
158.0
9.0
42.5
139.1
165.8
3.3
G16-13
691
6402
6.9
20.0960
2.9
0.1760
2.9
0.0257
0.5
0.17
163.3
0.8
164.6
4.4
183.8
66.5
163.3
0.8
G16-14
592
2238
2.5
20.0069
4.6
0.1640
4.7
0.0238
0.9
0.19
151.6
1.4
154.2
6.8
194.2
108.0
151.6
1.4
G16-15
730
8774
2.6
20.4746
2.3
0.1711
2.4
0.0254
0.7
0.29
161.8
1.1
160.4
3.6
140.2
54.5
161.8
1.1
G16-16
546
6842
3.2
19.8840
2.7
0.1803
2.9
0.0260
1.2
0.42
165.4
2.0
168.3
4.6
208.5
62.1
165.4
2.0
G16-17
429
3474
3.5
20.6620
3.0
0.1714
3.4
0.0257
1.6
0.48
163.5
2.6
160.6
5.0
118.8
70.4
163.5
2.6
G16-18
586
7302
2.4
20.3948
2.6
0.1746
2.6
0.0258
0.6
0.23
164.4
1.0
163.4
4.0
149.3
60.3
164.4
1.0
G16-19
1347
9626
7.7
20.1695
1.5
0.1732
1.7
0.0253
0.8
0.47
161.3
1.2
162.2
2.5
175.3
34.4
161.3
1.2
G16-20
2197
4286
2.5
17.5811
10.2
0.1891
11.2
0.0241
4.7
0.42
153.6
7.1
175.8
18.2
486.8
225.9
153.6
7.1
G16-21
406
4094
3.6
20.3556
5.0
0.1722
5.2
0.0254
1.6
0.30
161.8
2.5
161.3
7.8
153.9
116.4
161.8
2.5
G16-22
563
7864
5.1
20.0729
3.9
0.1747
4.1
0.0254
1.3
0.32
161.9
2.1
163.5
6.2
186.5
89.9
161.9
2.1
G16-23
427
4488
3.3
19.9975
5.2
0.1767
5.3
0.0256
0.9
0.17
163.1
1.5
165.2
8.1
195.3
121.7
163.1
1.5
G16-24
725
6966
2.0
20.2096
2.7
0.1730
3.2
0.0254
1.7
0.54
161.4
2.7
162.0
4.8
170.7
63.3
161.4
2.7
G16-25
452
3974
2.7
20.1687
3.5
0.1778
4.5
0.0260
2.8
0.62
165.5
4.6
166.2
6.9
175.4
82.3
165.5
4.6
G17-1
479
5942
2.3
20.4287
3.5
0.1567
3.7
0.0232
0.9
0.25
148.0
1.3
147.8
5.0
145.4
83.1
148.0
1.3
G17-2
390
4020
2.2
20.2985
5.1
0.1603
5.2
0.0236
0.6
0.12
150.3
0.9
150.9
7.2
160.4
119.8
150.3
0.9
G17-3
609
5314
1.9
19.9624
6.3
0.1663
6.3
0.0241
0.5
0.08
153.4
0.8
156.2
9.2
199.3
147.1
153.4
0.8
G17-4
444
3956
2.2
20.9930
3.2
0.1520
3.4
0.0231
1.2
0.36
147.5
1.8
143.7
4.6
81.2
75.2
147.5
1.8
G17-5
826
8142
2.7
19.8691
1.6
0.1582
2.1
0.0228
1.2
0.60
145.3
1.8
149.1
2.9
210.2
38.0
145.3
1.8
G17-6
571
6288
3.1
20.0140
2.0
0.1553
2.5
0.0225
1.5
0.59
143.7
2.1
146.5
3.4
193.3
46.0
143.7
2.1
G17-7
430
5058
2.7
19.6657
4.7
0.1663
4.7
0.0237
0.5
0.11
151.2
0.7
156.2
6.8
234.0
108.5
151.2
0.7
G17-8
519
6420
3.1
20.6411
1.4
0.1551
1.7
0.0232
0.9
0.56
148.0
1.4
146.4
2.3
121.1
32.4
148.0
1.4
G17-9
352
3638
2.4
21.0205
3.8
0.1528
4.0
0.0233
1.3
0.33
148.4
1.9
144.4
5.4
78.0
89.8
148.4
1.9
G17-10
653
5364
2.0
20.6243
2.5
0.1543
2.5
0.0231
0.6
0.23
147.1
0.8
145.7
3.5
123.0
58.4
147.1
0.8
44
G17-11
695
7444
1.6
20.0132
1.1
0.1614
1.7
0.0234
1.3
0.76
149.3
1.8
151.9
2.3
193.4
25.1
149.3
1.8
G17-12
714
8664
1.5
20.1649
3.0
0.1592
3.4
0.0233
1.4
0.42
148.4
2.1
150.0
4.7
175.9
71.1
148.4
2.1
G17-13
736
8390
5.2
20.5275
2.4
0.1532
2.5
0.0228
0.6
0.25
145.3
0.9
144.7
3.3
134.1
56.3
145.3
0.9
G17-14
451
5288
2.7
20.6618
3.7
0.1547
4.0
0.0232
1.4
0.35
147.7
2.0
146.0
5.4
118.8
87.7
147.7
2.0
G17-15
385
4346
2.1
20.7792
4.3
0.1546
4.3
0.0233
0.5
0.12
148.5
0.7
146.0
5.9
105.4
101.2
148.5
0.7
G17-16
529
5922
1.8
20.8817
2.7
0.1566
3.0
0.0237
1.1
0.38
151.1
1.7
147.7
4.1
93.8
64.9
151.1
1.7
G17-17
508
6450
3.5
19.5373
3.4
0.1643
3.5
0.0233
0.9
0.27
148.4
1.4
154.5
5.0
249.1
77.2
148.4
1.4
G17-18
515
6022
2.4
20.7291
2.8
0.1535
2.9
0.0231
0.9
0.29
147.1
1.2
145.0
4.0
111.1
66.5
147.1
1.2
G17-19
514
6874
2.8
20.0380
2.9
0.1610
3.0
0.0234
0.6
0.19
149.1
0.8
151.6
4.2
190.6
67.9
149.1
0.8
G17-20
473
4700
2.3
20.3072
3.6
0.1618
3.7
0.0238
0.5
0.14
151.8
0.8
152.3
5.2
159.4
84.9
151.8
0.8
G17-21
536
5592
2.5
20.6462
2.5
0.1558
2.8
0.0233
1.3
0.48
148.7
2.0
147.1
3.8
120.5
57.8
148.7
2.0
G17-22
496
5492
2.4
20.1607
5.8
0.1583
5.8
0.0231
0.6
0.10
147.5
0.8
149.2
8.1
176.3
134.9
147.5
0.8
G17-23
420
4644
2.2
20.4803
8.1
0.1570
8.2
0.0233
1.0
0.13
148.6
1.5
148.1
11.3
139.5
191.4
148.6
1.5
G17-24
436
5210
2.6
19.2484
5.5
0.1671
5.6
0.0233
1.0
0.18
148.6
1.5
156.9
8.2
283.3
126.3
148.6
1.5
G17-25
490
5058
3.0
20.1811
4.7
0.1584
4.7
0.0232
0.7
0.16
147.7
1.1
149.3
6.6
174.0
108.9
147.7
1.1
G18-1
3063
8336
1.8
18.4042
6.1
0.1490
6.3
0.0199
1.7
0.27
126.9
2.1
141.0
8.4
385.0
137.5
126.9
2.1
G18-2
525
6172
1.9
20.4735
4.0
0.1318
4.5
0.0196
2.0
0.44
124.9
2.4
125.7
5.3
140.3
94.7
124.9
2.4
G18-3
333
3816
2.6
19.1444
7.4
0.1410
7.6
0.0196
1.8
0.23
125.0
2.2
133.9
9.6
295.7
169.6
125.0
2.2
G18-4
397
3402
2.6
17.2389
15.4
0.1538
15.8
0.0192
3.1
0.20
122.8
3.8
145.3
21.3
530.1
340.1
122.8
3.8
G18-5
1202
13184
2.6
19.7447
3.5
0.1390
3.6
0.0199
0.9
0.24
127.1
1.1
132.2
4.5
224.8
82.0
127.1
1.1
G18-6
1722
11722
2.2
19.8813
1.9
0.1314
2.7
0.0190
1.9
0.70
121.0
2.2
125.4
3.2
208.8
44.6
121.0
2.2
G18-7
1794
10180
2.3
19.5298
1.8
0.1327
2.1
0.0188
1.1
0.52
120.1
1.3
126.5
2.5
250.0
40.9
120.1
1.3
G18-8
595
5538
1.8
20.8394
2.0
0.1156
4.4
0.0175
3.9
0.89
111.6
4.4
111.1
4.6
98.6
46.9
111.6
4.4
G18-9
714
8272
2.6
20.7956
2.6
0.1175
2.7
0.0177
0.6
0.21
113.3
0.6
112.8
2.8
103.5
61.3
113.3
0.6
G18-10
612
8576
2.2
20.4350
4.5
0.1259
4.8
0.0187
1.5
0.31
119.2
1.7
120.5
5.4
144.7
106.7
119.2
1.7
G18-11
2525
8640
2.4
18.5857
4.7
0.1440
5.4
0.0194
2.7
0.51
123.9
3.4
136.6
6.9
362.9
105.6
123.9
3.4
G18-12
389
4528
1.7
19.7338
5.8
0.1370
5.8
0.0196
0.5
0.09
125.2
0.6
130.4
7.1
226.0
134.1
125.2
0.6
G18-13
147
1982
1.4
15.4457
16.5
0.1682
17.7
0.0188
6.3
0.36
120.3
7.5
157.8
25.9
766.0
350.6
120.3
7.5
G18-14
623
6250
1.8
19.2561
10.3
0.1464
10.3
0.0204
0.7
0.07
130.4
1.0
138.7
13.4
282.4
236.4
130.4
1.0
G18-15
563
3806
2.1
18.7849
6.1
0.1405
6.5
0.0191
2.3
0.35
122.3
2.8
133.5
8.2
338.8
138.1
122.3
2.8
G18-16
1628
12088
2.1
19.6601
1.5
0.1362
2.5
0.0194
2.0
0.81
124.0
2.5
129.7
3.1
234.7
33.9
124.0
2.5
G18-17
630
5626
3.5
19.3820
7.3
0.1253
8.1
0.0176
3.6
0.44
112.6
4.0
119.9
9.2
267.5
167.3
112.6
4.0
45
G18-18
2435
16768
6.1
19.8023
4.0
0.1426
5.3
0.0205
3.5
0.65
130.7
4.5
135.4
6.7
218.0
92.7
130.7
4.5
G18-19
832
8344
2.7
19.6481
2.3
0.1348
3.1
0.0192
2.1
0.68
122.7
2.6
128.4
3.8
236.1
53.0
122.7
2.6
G18-20
220
2782
1.3
19.4801
6.3
0.1391
6.4
0.0197
1.2
0.18
125.5
1.4
132.3
8.0
255.9
145.3
125.5
1.4
G18-21
2005
17554
2.7
20.1963
3.1
0.1315
3.5
0.0193
1.6
0.46
123.0
2.0
125.4
4.2
172.2
73.2
123.0
2.0
G18-22
765
7822
2.2
19.1663
3.3
0.1420
3.5
0.0197
1.2
0.34
126.0
1.5
134.8
4.5
293.1
75.8
126.0
1.5
G18-23
443
4292
1.6
18.2881
6.6
0.1575
6.6
0.0209
1.0
0.15
133.3
1.3
148.5
9.2
399.2
147.2
133.3
1.3
G18-24
1309
10134
2.1
20.7125
2.3
0.1350
3.1
0.0203
2.1
0.67
129.4
2.7
128.6
3.8
113.0
54.7
129.4
2.7
G18-25
607
6760
2.3
20.7301
2.5
0.1251
3.0
0.0188
1.6
0.52
120.1
1.9
119.7
3.4
111.0
59.8
120.1
1.9
G19-1
299
4034
2.4
19.0898
4.3
0.1151
4.6
0.0159
1.5
0.33
101.9
1.5
110.6
4.8
302.2
98.6
101.9
1.5
G19-2
186
2538
2.4
19.5768
10.0
0.1132
10.1
0.0161
1.4
0.13
102.8
1.4
108.9
10.4
244.5
230.3
102.8
1.4
G19-3
224
3028
2.2
19.5151
8.3
0.1171
8.4
0.0166
0.9
0.11
106.0
1.0
112.5
8.9
251.7
192.4
106.0
1.0
G19-4
157
1984
2.2
19.0144
16.1
0.1155
16.2
0.0159
1.9
0.11
101.9
1.9
111.0
17.1
311.2
369.4
101.9
1.9
G19-5
210
2034
2.4
21.1328
22.8
0.1069
22.8
0.0164
1.0
0.04
104.8
1.1
103.2
22.3
65.4
547.8
104.8
1.1
G19-6
252
2660
2.2
19.3797
3.2
0.1151
3.3
0.0162
0.5
0.16
103.5
0.5
110.7
3.4
267.7
74.1
103.5
0.5
G19-7
205
1836
1.7
21.6061
9.0
0.1020
9.2
0.0160
1.6
0.17
102.2
1.6
98.6
8.6
12.4
217.6
102.2
1.6
G19-8
240
2506
2.0
18.9900
5.4
0.1226
5.5
0.0169
1.3
0.24
108.0
1.4
117.5
6.1
314.1
122.0
108.0
1.4
G19-9
255
2570
1.2
19.6379
8.7
0.1168
8.7
0.0166
0.8
0.09
106.4
0.9
112.2
9.2
237.3
200.3
106.4
0.9
G19-10
215
2424
1.9
20.8061
10.4
0.1090
10.4
0.0164
0.6
0.06
105.1
0.6
105.0
10.4
102.3
246.3
105.1
0.6
G19-11
227
2736
2.2
23.0593
13.8
0.0988
13.9
0.0165
1.6
0.11
105.6
1.6
95.6
12.7
-146.5
344.3
105.6
1.6
G19-12
127
1384
1.8
17.4020
13.5
0.1313
13.6
0.0166
1.2
0.09
105.9
1.3
125.3
16.0
509.4
298.7
105.9
1.3
G19-13
186
1922
1.6
19.6261
8.9
0.1151
9.0
0.0164
1.4
0.15
104.8
1.4
110.6
9.5
238.7
206.3
104.8
1.4
G19-14
204
1870
1.8
19.7351
10.3
0.1122
10.4
0.0161
1.5
0.15
102.7
1.6
107.9
10.6
225.9
238.1
102.7
1.6
G19-15
211
2726
2.0
20.8576
12.4
0.1076
12.5
0.0163
1.6
0.13
104.1
1.6
103.8
12.3
96.5
293.5
104.1
1.6
G19-16
262
3486
2.5
20.2691
8.8
0.1128
8.9
0.0166
1.3
0.15
106.0
1.4
108.5
9.1
163.8
205.2
106.0
1.4
G19-17
149
1470
1.7
19.9480
14.7
0.1174
14.8
0.0170
1.9
0.13
108.6
2.1
112.7
15.8
201.0
342.5
108.6
2.1
G19-178
108
1328
1.5
21.5372
28.5
0.1063
28.6
0.0166
1.7
0.06
106.1
1.8
102.6
27.9
20.0
697.8
106.1
1.8
G19-19
293
2488
2.2
18.8234
9.8
0.1230
9.9
0.0168
1.6
0.16
107.4
1.7
117.8
11.0
334.1
222.0
107.4
1.7
G19-20
370
3600
2.4
20.0989
3.2
0.1122
3.5
0.0164
1.4
0.40
104.6
1.5
108.0
3.6
183.5
75.3
104.6
1.5
G19-21
179
2116
2.5
16.4662
18.9
0.1409
19.4
0.0168
4.2
0.22
107.6
4.5
133.8
24.3
629.7
410.5
107.6
4.5
G19-22
296
3818
1.6
18.8203
7.7
0.1231
7.7
0.0168
0.6
0.08
107.4
0.7
117.9
8.6
334.5
175.3
107.4
0.7
G19-23
177
1998
2.2
18.8484
13.0
0.1258
13.1
0.0172
1.8
0.14
109.9
1.9
120.3
14.8
331.1
295.2
109.9
1.9
G19-24
227
2570
1.5
20.8284
6.7
0.1137
6.9
0.0172
1.3
0.19
109.8
1.4
109.4
7.1
99.8
159.4
109.8
1.4
46
G19-25
143
1622
1.8
17.9945
12.4
0.1254
12.5
0.0164
1.3
0.10
104.6
1.3
119.9
14.1
435.3
278.0
104.6
1.3
G20-1
585
2194
2.9
21.4029
5.0
0.1018
5.3
0.0158
1.6
0.30
101.0
1.6
98.4
4.9
35.1
119.9
101.0
1.6
G20-2
316
2406
3.7
22.5152
15.2
0.0982
15.4
0.0160
2.3
0.15
102.5
2.3
95.1
13.9
-87.6
374.2
102.5
2.3
G20-3
467
2940
2.7
20.8162
6.3
0.1031
6.8
0.0156
2.7
0.39
99.6
2.6
99.6
6.5
101.2
148.7
99.6
2.6
G20-4
552
1364
1.4
17.7643
12.1
0.1244
12.3
0.0160
1.8
0.15
102.5
1.9
119.1
13.8
463.9
269.3
102.5
1.9
G20-5
402
2326
3.4
22.4995
8.7
0.0962
8.9
0.0157
1.7
0.19
100.4
1.7
93.3
7.9
-85.9
214.4
100.4
1.7
G20-6
756
4440
1.4
20.9948
2.9
0.1053
4.9
0.0160
4.0
0.82
102.5
4.1
101.6
4.8
81.0
67.7
102.5
4.1
G20-7
416
1914
3.4
21.9379
7.2
0.1003
7.3
0.0160
1.2
0.16
102.1
1.2
97.1
6.7
-24.4
174.3
102.1
1.2
G20-8
389
1982
0.8
20.9939
8.2
0.1043
9.0
0.0159
3.7
0.41
101.6
3.7
100.8
8.6
81.1
194.4
101.6
3.7
G20-89
858
4176
2.5
21.2655
5.7
0.1047
5.9
0.0161
1.5
0.26
103.3
1.6
101.1
5.6
50.5
135.4
103.3
1.6
G20-10
460
2238
2.4
20.6961
5.7
0.1085
5.8
0.0163
1.1
0.18
104.1
1.1
104.6
5.8
114.9
135.4
104.1
1.1
G20-11
471
2318
3.2
21.8796
5.4
0.0994
5.7
0.0158
1.8
0.31
100.9
1.8
96.2
5.2
-17.9
130.6
100.9
1.8
G20-12
672
3168
2.6
20.7491
4.9
0.1071
5.1
0.0161
1.4
0.27
103.0
1.4
103.3
5.0
108.8
116.8
103.0
1.4
G20-13
488
2040
3.0
21.3666
4.8
0.1024
4.9
0.0159
0.8
0.15
101.5
0.8
99.0
4.6
39.1
115.6
101.5
0.8
G20-14
631
2610
1.5
20.8178
9.7
0.1027
9.8
0.0155
1.0
0.10
99.2
1.0
99.3
9.2
101.0
230.1
99.2
1.0
G20-15
573
2714
1.9
21.5886
5.4
0.1002
5.7
0.0157
1.7
0.30
100.3
1.7
96.9
5.2
14.3
130.0
100.3
1.7
G20-16
648
2536
2.9
21.0142
4.5
0.1034
4.6
0.0158
0.7
0.15
100.8
0.7
99.9
4.4
78.8
108.0
100.8
0.7
G20-17
339
1988
1.8
22.1849
7.2
0.0984
7.3
0.0158
1.1
0.15
101.3
1.1
95.3
6.6
-51.6
175.8
101.3
1.1
G20-18
597
2148
2.9
20.7798
3.8
0.1068
4.0
0.0161
1.2
0.30
103.0
1.2
103.1
3.9
105.3
90.1
103.0
1.2
G20-19
509
2076
3.2
21.1116
5.7
0.1030
5.8
0.0158
1.0
0.17
100.9
1.0
99.6
5.5
67.8
136.6
100.9
1.0
G20-20
534
2116
3.5
20.7204
7.1
0.1037
7.9
0.0156
3.4
0.43
99.7
3.4
100.2
7.5
112.1
168.5
99.7
3.4
G20-21
791
3898
2.5
21.1378
3.5
0.1027
3.7
0.0157
1.4
0.37
100.7
1.4
99.3
3.5
64.8
82.4
100.7
1.4
G20-22
530
2088
3.3
20.3717
8.3
0.1084
8.4
0.0160
1.6
0.18
102.4
1.6
104.5
8.3
152.0
193.7
102.4
1.6
G20-23
931
4866
2.0
20.9991
2.8
0.1046
3.1
0.0159
1.1
0.37
101.8
1.2
101.0
2.9
80.5
67.3
101.8
1.2
G20-24
652
3176
3.0
20.8684
10.6
0.1054
10.8
0.0160
1.8
0.16
102.1
1.8
101.8
10.4
95.3
252.0
102.1
1.8
G20-25
528
2444
3.0
21.7768
4.9
0.1019
5.1
0.0161
1.5
0.29
102.9
1.5
98.5
4.8
-6.6
117.8
102.9
1.5
G20-26
539
1164
2.8
19.8092
11.9
0.1190
11.9
0.0171
0.5
0.04
109.3
0.5
114.2
12.9
217.2
276.9
109.3
0.5
G20-27
548
2498
3.1
21.4078
5.2
0.1064
5.3
0.0165
0.9
0.18
105.6
1.0
102.7
5.1
34.5
124.1
105.6
1.0
G20-28
238
1652
2.3
22.5329
14.0
0.0959
14.1
0.0157
1.7
0.12
100.3
1.7
93.0
12.5
-89.6
344.7
100.3
1.7
G20-29
713
3026
2.4
21.2545
3.5
0.1015
4.3
0.0156
2.6
0.60
100.1
2.6
98.1
4.0
51.7
82.8
100.1
2.6
G20-30
485
1532
2.8
20.4429
15.0
0.1067
15.2
0.0158
2.5
0.17
101.1
2.5
102.9
14.8
143.8
352.6
101.1
2.5
G21-1
373
2632
2.2
22.2911
9.2
0.1053
9.4
0.0170
2.0
0.21
108.8
2.2
101.6
9.1
-63.2
224.0
108.8
2.2
47
G21-2
406
2622
1.7
21.0458
11.7
0.1159
11.7
0.0177
0.8
0.07
113.1
0.9
111.4
12.3
75.2
277.8
113.1
0.9
G21-3
274
1882
2.5
21.6853
5.4
0.1081
5.5
0.0170
0.7
0.12
108.7
0.7
104.2
5.4
3.6
131.2
108.7
0.7
G21-4
556
3240
4.2
20.9968
7.6
0.1169
7.6
0.0178
0.9
0.12
113.7
1.0
112.2
8.1
80.7
179.6
113.7
1.0
G21-5
635
4288
1.5
21.1499
2.1
0.1152
2.6
0.0177
1.5
0.57
112.9
1.6
110.7
2.7
63.5
50.3
112.9
1.6
G21-6
297
2122
2.5
21.3034
3.2
0.1138
3.4
0.0176
1.1
0.33
112.4
1.2
109.5
3.6
46.2
77.6
112.4
1.2
G21-7
630
4930
1.6
21.1913
3.9
0.1144
4.1
0.0176
0.9
0.23
112.3
1.0
109.9
4.2
58.8
94.0
112.3
1.0
G21-8
178
714
2.1
21.0104
29.2
0.1121
29.3
0.0171
1.9
0.07
109.2
2.1
107.9
30.0
79.2
707.6
109.2
2.1
G21-9
279
1930
2.6
21.9376
5.6
0.1035
5.8
0.0165
1.4
0.24
105.3
1.5
100.0
5.5
-24.3
136.6
105.3
1.5
G21-10
259
1942
2.2
22.1083
7.3
0.1069
7.4
0.0171
0.9
0.12
109.6
1.0
103.2
7.2
-43.2
177.8
109.6
1.0
G21-11
246
1728
1.8
22.7529
9.5
0.1045
9.7
0.0173
1.5
0.16
110.3
1.7
101.0
9.3
-113.5
235.3
110.3
1.7
G21-12
319
2116
2.1
22.1442
7.6
0.1097
7.6
0.0176
1.1
0.14
112.6
1.2
105.7
7.7
-47.1
184.4
112.6
1.2
G21-13
272
1280
2.0
19.7647
7.6
0.1201
7.6
0.0172
0.5
0.07
110.1
0.5
115.2
8.3
222.4
175.7
110.1
0.5
G21-14
158
1428
2.1
21.7934
8.5
0.1073
9.1
0.0170
3.3
0.36
108.4
3.5
103.4
9.0
-8.4
205.5
108.4
3.5
G21-15
277
2586
2.0
22.1476
6.6
0.1080
7.0
0.0173
2.5
0.35
110.8
2.7
104.1
6.9
-47.5
159.8
110.8
2.7
G21-16
177
1606
2.3
22.2073
8.0
0.1027
8.1
0.0165
0.8
0.10
105.7
0.8
99.2
7.6
-54.0
196.2
105.7
0.8
G21-17
331
2630
2.5
21.6016
5.1
0.1051
5.3
0.0165
1.3
0.25
105.3
1.4
101.4
5.1
12.9
123.4
105.3
1.4
G21-18
185
1470
3.3
22.4810
9.6
0.1039
9.8
0.0169
2.2
0.22
108.3
2.3
100.4
9.4
-83.9
235.0
108.3
2.3
G21-19
219
1672
2.2
23.3851
13.7
0.1030
13.7
0.0175
0.7
0.05
111.7
0.7
99.6
13.0
-181.4
342.2
111.7
0.7
G21-20
241
2046
3.1
20.8929
8.5
0.1124
8.8
0.0170
2.4
0.27
108.9
2.6
108.1
9.0
92.5
201.2
108.9
2.6
G21-21
200
2020
2.9
22.8396
10.9
0.1002
11.0
0.0166
1.3
0.12
106.1
1.3
97.0
10.1
-122.8
269.1
106.1
1.3
G21-22
259
2172
2.9
21.4677
6.2
0.1049
6.6
0.0163
2.0
0.30
104.4
2.1
101.3
6.3
27.8
149.9
104.4
2.1
G21-23
381
3258
3.2
21.6012
4.5
0.1075
4.8
0.0168
1.6
0.33
107.6
1.7
103.6
4.7
12.9
107.8
107.6
1.7
G21-24
497
4034
2.2
21.0274
3.3
0.1089
3.6
0.0166
1.2
0.35
106.2
1.3
105.0
3.6
77.3
79.4
106.2
1.3
G21-25
359
2996
3.6
21.6022
4.8
0.0985
5.9
0.0154
3.5
0.59
98.8
3.4
95.4
5.4
12.8
115.0
98.8
3.4
G22-1
860
8576
4.2
20.5845
4.3
0.0988
4.4
0.0148
0.8
0.19
94.4
0.8
95.7
4.0
127.6
101.0
94.4
0.8
G22-2
1015
8670
2.2
19.8142
3.7
0.1011
4.1
0.0145
1.6
0.40
93.0
1.5
97.8
3.8
216.6
86.2
93.0
1.5
G22-3
521
3898
0.9
20.5476
5.7
0.0950
6.2
0.0142
2.3
0.37
90.7
2.1
92.2
5.5
131.8
135.0
90.7
2.1
G22-4
963
7748
2.1
20.2347
3.6
0.0953
3.8
0.0140
1.2
0.32
89.5
1.1
92.4
3.4
167.8
84.9
89.5
1.1
G22-5
737
7784
2.1
19.8283
2.6
0.1000
2.9
0.0144
1.3
0.46
92.0
1.2
96.8
2.7
215.0
59.1
92.0
1.2
G22-6
414
3338
2.4
18.8575
6.2
0.1047
6.5
0.0143
1.8
0.28
91.7
1.6
101.1
6.2
330.0
141.3
91.7
1.6
G22-8
1248
8096
1.5
20.1899
2.7
0.0974
3.2
0.0143
1.7
0.53
91.2
1.5
94.3
2.8
173.0
62.6
91.2
1.5
G22-9
674
5138
1.6
20.9201
5.2
0.0934
5.3
0.0142
0.7
0.14
90.8
0.7
90.7
4.6
89.4
124.0
90.8
0.7
48
G22-7
614
4164
1.4
20.0640
5.2
0.0937
5.3
0.0136
1.2
0.22
87.3
1.0
91.0
4.6
187.5
121.2
87.3
1.0
G22-10
529
4926
2.2
20.9420
7.1
0.0907
7.2
0.0138
1.2
0.16
88.2
1.0
88.1
6.0
86.9
167.8
88.2
1.0
G22-11
596
5324
2.1
21.2724
2.9
0.0918
3.3
0.0142
1.5
0.45
90.7
1.3
89.2
2.8
49.7
69.6
90.7
1.3
G22-12
716
6922
1.5
20.9120
3.9
0.0933
4.3
0.0141
1.7
0.40
90.5
1.5
90.5
3.7
90.3
92.8
90.5
1.5
G22-13
671
6262
2.0
20.6515
4.9
0.0931
5.3
0.0139
2.0
0.38
89.2
1.8
90.4
4.6
119.9
115.5
89.2
1.8
G22-14
580
5076
1.6
20.3881
4.3
0.0944
4.6
0.0140
1.6
0.35
89.4
1.4
91.6
4.0
150.1
101.6
89.4
1.4
G22-15
249
2252
1.7
18.0262
21.6
0.1082
21.6
0.0141
1.5
0.07
90.6
1.3
104.3
21.4
431.4
485.9
90.6
1.3
G22-16
509
4704
1.6
19.9734
7.5
0.1011
8.0
0.0146
2.7
0.33
93.7
2.5
97.8
7.4
198.1
174.6
93.7
2.5
G22-17
387
3424
1.7
20.2701
10.6
0.0910
10.8
0.0134
2.3
0.21
85.6
1.9
88.4
9.2
163.7
248.2
85.6
1.9
G22-18
808
5278
1.4
19.7095
3.3
0.1012
3.4
0.0145
0.8
0.24
92.6
0.8
97.9
3.2
228.9
77.2
92.6
0.8
G22-19
536
5232
3.9
19.4997
14.3
0.1104
14.4
0.0156
1.6
0.11
99.9
1.6
106.4
14.5
253.5
329.9
99.9
1.6
G22-20
552
5728
2.1
20.4177
2.8
0.0943
4.4
0.0140
3.5
0.78
89.4
3.1
91.5
3.9
146.7
65.0
89.4
3.1
G22-21
1253
8666
1.8
20.4172
2.7
0.0921
3.2
0.0136
1.6
0.51
87.3
1.4
89.5
2.7
146.8
64.0
87.3
1.4
G22-22
507
4226
2.8
20.5238
6.4
0.0896
6.7
0.0133
2.1
0.31
85.4
1.7
87.1
5.6
134.5
150.5
85.4
1.7
G22-23
422
4758
2.6
20.7898
6.2
0.0935
6.3
0.0141
0.8
0.12
90.3
0.7
90.8
5.4
104.2
146.9
90.3
0.7
G22-24
988
8106
1.1
20.4757
2.6
0.0923
3.1
0.0137
1.8
0.58
87.7
1.6
89.6
2.7
140.1
59.9
87.7
1.6
G22-25
295
2516
2.0
19.5238
8.0
0.0965
8.1
0.0137
1.2
0.15
87.5
1.1
93.6
7.3
250.7
185.3
87.5
1.1
G23-1
882
3958
2.8
20.8425
3.2
0.1107
3.9
0.0167
2.2
0.56
107.0
2.3
106.6
3.9
98.2
76.4
107.0
2.3
G23-3
632
1962
2.6
19.5169
6.9
0.1165
7.0
0.0165
1.2
0.17
105.5
1.2
111.9
7.4
251.5
158.7
105.5
1.2
G23-4
1206
4944
2.3
20.7693
2.3
0.1094
3.2
0.0165
2.3
0.71
105.4
2.4
105.4
3.2
106.5
53.9
105.4
2.4
G23-6
1138
4102
2.4
20.9693
5.4
0.1083
5.5
0.0165
1.4
0.25
105.3
1.4
104.4
5.5
83.8
127.2
105.3
1.4
G23-7
319
1670
2.4
20.4236
12.6
0.1104
13.5
0.0164
4.6
0.34
104.6
4.8
106.4
13.6
146.0
297.4
104.6
4.8
G23-8
951
3460
2.7
19.1533
6.3
0.1169
6.7
0.0162
2.0
0.30
103.8
2.1
112.2
7.1
294.6
144.9
103.8
2.1
G23-9
340
1538
2.4
21.5049
11.9
0.1066
12.0
0.0166
1.0
0.08
106.3
1.1
102.9
11.7
23.7
286.6
106.3
1.1
G23-10
726
3558
3.0
21.1292
3.2
0.1074
4.7
0.0165
3.4
0.72
105.2
3.5
103.6
4.6
65.8
77.0
105.2
3.5
G23-11
1220
4912
2.9
20.6486
5.7
0.1137
5.8
0.0170
1.4
0.24
108.9
1.5
109.4
6.0
120.3
133.4
108.9
1.5
G23-12
965
4420
2.8
21.0911
2.8
0.1113
4.4
0.0170
3.4
0.78
108.8
3.7
107.2
4.5
70.1
65.6
108.8
3.7
G23-13
1186
5744
2.8
20.3838
1.2
0.1146
2.4
0.0169
2.0
0.86
108.3
2.2
110.2
2.5
150.6
27.7
108.3
2.2
G23-14
561
3098
2.7
21.8621
6.0
0.1031
6.2
0.0163
1.2
0.19
104.5
1.2
99.6
5.8
-16.0
146.2
104.5
1.2
G23-15
569
2682
2.8
21.1722
5.8
0.1091
5.9
0.0168
1.2
0.20
107.1
1.3
105.2
5.9
60.9
138.3
107.1
1.3
G23-16
933
3858
3.3
19.7994
14.3
0.1172
14.6
0.0168
2.8
0.19
107.6
3.0
112.5
15.5
218.4
332.8
107.6
3.0
G23-2
394
2032
3.3
21.5457
7.4
0.1070
7.6
0.0167
1.7
0.22
106.9
1.8
103.2
7.4
19.1
177.0
106.9
1.8
49
G23-5
656
3578
2.3
20.7125
5.3
0.1095
5.6
0.0164
1.6
0.29
105.1
1.7
105.5
5.6
113.0
126.2
105.1
1.7
G23-17
480
2576
2.7
21.0410
5.2
0.1067
6.1
0.0163
3.1
0.51
104.1
3.2
102.9
5.9
75.7
123.9
104.1
3.2
G23-18
768
3466
2.7
21.1437
3.8
0.1118
3.8
0.0171
0.5
0.13
109.6
0.5
107.6
3.9
64.2
90.1
109.6
0.5
G23-19
906
4226
2.0
21.2982
2.7
0.1089
3.0
0.0168
1.3
0.44
107.5
1.4
105.0
3.0
46.8
64.9
107.5
1.4
G23-20
1019
4950
2.4
20.8207
3.3
0.1110
3.4
0.0168
0.5
0.15
107.2
0.5
106.9
3.4
100.7
79.0
107.2
0.5
G23-21
414
2484
2.6
19.0152
11.3
0.1286
11.3
0.0177
1.0
0.09
113.3
1.2
122.8
13.1
311.1
257.5
113.3
1.2
G23-22
911
4190
2.8
20.6074
4.4
0.1109
4.5
0.0166
1.0
0.23
106.0
1.1
106.8
4.5
125.0
102.6
106.0
1.1
G23-23
1030
4490
0.8
21.1152
2.4
0.1079
2.8
0.0165
1.3
0.48
105.7
1.4
104.1
2.7
67.4
57.6
105.7
1.4
G23-24
437
2068
2.8
20.7196
13.5
0.1071
13.5
0.0161
0.8
0.06
102.9
0.8
103.3
13.2
112.2
318.9
102.9
0.8
G23-26
761
3522
2.5
20.3774
4.6
0.1127
4.8
0.0166
1.3
0.28
106.4
1.4
108.4
4.9
151.3
107.5
106.4
1.4
G23-27
1234
4722
2.2
20.7984
3.0
0.1106
3.8
0.0167
2.4
0.63
106.7
2.5
106.5
3.8
103.2
69.8
106.7
2.5
G23-28
1406
5140
2.0
20.2107
2.7
0.1149
3.2
0.0168
1.7
0.52
107.7
1.8
110.4
3.4
170.6
63.9
107.7
1.8
G23-29
693
4276
2.1
20.8967
2.0
0.1098
3.0
0.0166
2.3
0.75
106.3
2.4
105.7
3.1
92.1
47.3
106.3
2.4
G23-30
455
2020
1.9
21.8220
4.8
0.1037
5.3
0.0164
2.1
0.39
104.9
2.2
100.2
5.0
-11.6
116.9
104.9
2.2
50
Table 3. Age determinations from
U-Pb geochronologic analyses.
Best age
±
Sample
(Ma)
(Ma)
Northern Transect
G01
162.1
3.5
G02
162.0
3.0
G03
166.8
2.3
G04
145.3
3.4
G05
G06
109.0
2.5
G08
370.4
7.2
G09
116.4
2.6
G10
111.6
2.6
G11
120.0
2.2
G12
Southern Transect
G14
165.4
2.2
G16
163.2
3.2
G17
148.7
2.7
G18
125.5
3.1
G19
105.2
1.5
G20
101.5
1.8
G21
109.8
2.6
G22
90.4
2.1
G23
106.8
2.0
51
Table 4. Sr and Nd isotopic data.
Sample Rock Type
Rb
(ppm)
Sr
(ppm)
87Rb/
86Sr
87Sr/
86Sr
87Sr/86Sr
Initial
Sm
(ppm)
Nd
(ppm)
147Sm/
144Nd
143Nd/
144Nd
143Nd/144Nd
Initial
eNd0
G01
G02
G03
G04
G05
G06
G08
G09
G10
G11
G12
granodiorite
granodiorite
granodiorite
granodiorite
tonalite
granodiorite
granite
granodiorite
granodiorite
granodiorite
diorite
46.437
32.695
40.382
190.236
62.952
76.292
88.340
77.439
67.427
20.894
194.819
195.154
370.074
30.683
387.796
404.447
338.082
438.150
402.435
557.205
0.6852
0.4816
0.3137
17.8753
0.4667
0.5423
0.7513
0.5082
0.4817
0.1078
0.7045
0.7045
0.7054
0.7346
0.7056
0.7057
0.7072
0.7063
0.7067
0.7050
0.7029
0.7034
0.7048
0.7080
0.7049
0.7028
0.7060
0.7055
0.7058
0.7048
1.366
2.606
2.284
4.372
1.936
6.139
2.167
2.635
3.432
2.521
2.436
6.655
10.583
21.932
9.458
9.115
33.394
11.242
11.936
17.167
12.727
10.661
0.1241
0.1489
0.0630
0.2794
0.1284
0.1111
0.1165
0.1334
0.1209
0.1197
0.1381
0.5128
0.5129
0.5125
0.5124
0.5127
0.5115
0.5126
0.5124
0.5125
0.5123
0.5126
0.5126
0.5128
0.5124
0.5122
0.5126
0.5114
0.5123
0.5123
0.5124
0.5123
0.5124
2.22
5.75
-2.61
-3.88
0.53
-22.63
-0.51
-4.35
-3.61
-5.66
-1.60
G14
G16
G17
G18
G19
G20
G21
G22
G23
granodiorite
granodiorite
granodiorite
tonalite
granodiorite
granodiorite
granodiorite
granodiorite
granodiorite
151.633
106.843
115.582
137.710
84.356
105.718
76.872
88.699
77.275
474.447
629.426
2.551
44.899
340.638
306.229
420.676
397.452
283.745
0.9190
0.4880
134.6140
8.8335
0.7120
0.9927
0.5254
0.6417
0.7830
0.7075
0.7062
1.0481
0.7238
0.7065
0.7074
0.7064
0.7064
0.7062
0.7054
0.7050
0.7417
0.7081
0.7054
0.7059
0.7056
0.7056
0.7050
6.053
4.316
8.828
2.851
2.082
2.742
2.663
2.317
3.094
29.785
22.454
43.280
13.006
10.323
15.383
14.208
13.828
13.991
0.1229
0.1162
0.1233
0.1325
0.1219
0.1078
0.1133
0.1013
0.1337
0.5125
0.5126
0.5126
0.5123
0.5124
0.5123
0.5124
0.5124
0.5126
0.5124
0.5125
0.5124
0.5122
0.5124
0.5123
0.5123
0.5124
0.5125
-2.91
-1.01
-1.42
-5.75
-3.73
-5.81
-5.23
-4.19
-1.11
52