The Rb-Sr method - Homepage Server Uni-Tübingen · 2019-06-26 · The Rb-Sr method is commonly...
Transcript of The Rb-Sr method - Homepage Server Uni-Tübingen · 2019-06-26 · The Rb-Sr method is commonly...
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The Rb-Sr method
Based on the decay reaction: with a half-life
T1/2 = 48.8 Ga geochronometry equation written in terms of the
ratio 87Sr/86Sr because ratios are more accurately determined by mass spectrometry
−+→ βSrRb 8738
8737
)1(86
87
086
87
86
87
−+
= te
SrRb
SrSr
SrSr λ
measured measured always some initial Sr present in a rock
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The Rb-Sr method is commonly used to date Rb-rich minerals such as muscovite, biotite and K-feldspar; these minerals usually do not incorporate much Sr at the time of their formation (Goldschmidt’s rules).
During the last decades also cogenetic whole
rock samples were analysed by this method.
The Rb-Sr method
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87Rb=27.83% 85Rb=72.17% 88Sr=82.53% 87Sr=7.04% 86Sr=9.87% 84Sr=0.56%
ALL STABLE
What accounts for huge range in Rb/Sr ratios of rocks? 1. Rb subsitutes for K in K-bearing minerals while Sr substitutes for Ca in Ca-bearing minerals 2. Rb and Sr are fractionated by igneous processes: Rb tends to prefer melt (more incompatible than Sr)
Rb/Sr ratios for various rocks: Ultrabasic 0.2 Basaltic 0.06 Granites 0.25-10 Shale 0.46 Sandstone 3
High Rb/Sr rocks contain more 87Sr Low Rb/Sr rocks contain less 87Sr
The Rb-Sr method
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Igneous Processes and 87Sr/86Sr ratios
87Sr/86Sr ratios of igneous rocks: MORB 0.7025 Ocean Islands >0.704 Continents 0.7119
87Rb goes into the melt
MORB
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igneous rocks are heterogeneous, different mineral phases will have different Rb/Sr ratios, even though they have the same crystallization age and the same 87Sr/86Sr initial
MANTLE 87Sr/86Sr = 0.702
ROCK (87Sr/86Sr) i= 0.702
Rb/Sr=0.6
Rb/Sr=1.2 Rb/Sr= 0.8
t=Ti
me
of
crys
talli
zatio
n
how to get the initial 87Sr/86Sr ratio?
The Rb-Sr method
usually the isochron method is employed to determine the age and initial 87Sr/86Sr ratio of a suite of rock samples
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87Rb/86Sr
y = 0.7114
0 5 10 15 20 25 30 350.70
0.75
0.80
0.85
0.90
0.95
87Sr
/86S
r
Rb-Sr isochron diagram for a series of cogenetic rock samples formed at the same time
( 87 Sr/ 86 Sr) 0 = 0.7114 slope = (e λ t - 1) = 0.04855
t = 3.34 Ga
r 2 = 0.9980 if x=(87Rb/86Sr)m
and y=(87Sr/86Sr)m
y=b+mx intercept b=(87Sr/86Sr)i
slope m=(eλt-1)
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Isochron (part II): regression treatment with pocket calculator
Exercise 11
sample 87Rb/86Sr 87Sr/86Sr L14 446.6 2.76164 L12 600.4 3.4311 L16 820.6 4.4054 L15 999.1 5.1927
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BABI - Basaltic Achondrite Best Initial = Bulk Earth, undifferentiated
Rb-Sr isochron from meteorites 87Sr/86Sr ratios of igneous rocks:
MORB 0.7025 Continents 0.7119 Ocean Islands >0.704 vs. Meteorites 0.699
T=4.5Ga
The Rb-Sr method
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87Rb/86Sr
87Sr
/86Sr
t = 0
t = t2
t = t1
M1 R2M2R1
M1
R2
M2R1
Rb-Sr isochron diagram illustrating how the isochron evolves as a function of time. M1 and M2 are cogenetic minerals and R1 and R2 are cogenetic rocks, all with different initial Rb/Sr ratios
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less thana few cm
several km
batholith
TimeTime
feldsparfeldspar
feldspar
whole rock
whole rock
whole rock
biotite
biotite
biotite
tm tm tp
to to
ri ri
rm
87Sr
/86S
r
87Sr
/86S
r
diffusion through crystal lattice and along grain boundaries during metamorphism
Response of Rb/Sr-system during metamorphism
Response of Rb/Sr-system during metamorphism
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Response of Rb/Sr-system during metamorphism
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Rb/Sr Rb/Sr
slope = e -1λti
slope = e -1λtm
fd fd
fd
wr wr
wr
bt bt
bt
rm rm
ri ri
87Sr
/86S
r
87Sr
/86S
r
TimeTime
feldsparfeldspar
feldspar
whole rock
whole rock
whole rock
biotite
biotite
biotite
tm tm tp
to to
ri ri
rm
87Sr
/86S
r
87Sr
/86S
r
Response of Rb/Sr-system during metamorphism
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Sr isotopic evolution of the Earth
time
crustextracted
crust
mantledepletedmantle87
Sr/8
6Sr
Rb
Sr
Rb Sr 87Sr/86Sr ratio of the crust is higher than that of the mantle due to the preferential partitioning of Rb into the crust relative to Sr.
Continental crust: 32-78 ppm Rb, 260-333 ppm Sr Depleted Mantle: 0.6 ppm Rb, 19.9 ppm Sr
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Age in Ga0 1 2 3 4
(87S
r/86S
r)
0.695
0.700
0.705
0.710
0.715
0.720
0.725
Tracking (87Sr/86Sr)i through time
BABI
Average continental crust
MORB
early continental differentiation
continuing continental growth
continuing upper mantle depletion
Ocean islands
(87Sr/86Sr)i ratios indicate how enriched or depleted its mantle source was i.e. (87Sr/86Sr)i = 0.7020 at 1 Ga means a depleted source (87Sr/86Sr)i value of 0.728 at 1 Ga?
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The evolution of 87Sr/86Sr with time in the continental crust and mantle
(87Sr/86Sr)0 ratios can be used as a tracer to determine if a magma evolved from the mantle or if crust was involved For mantle-derived rocks: (87Sr/86Sr)0 ≈ 0.700-0.706 For crustal involvement: (87Sr/86Sr)0 ≈ 0.705-0.740
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Sr isotopes as tracer of rock origin
U n d i f f e r e n t i a t e d e a r t h C r u s t a t 1 . 0 M a 8 7 8 6 S r / S r = 0 . 7 1 4 0
M a n t l e a t 1 . 0 M a 8 7 8 6 S r / S r = 0 . 7 0 3 4
c r u s t a n d m a n t l e d i f f e r e n t i a t e a t 2 . 7 M a
p r e s e n t d a y r o c k w i t h
( S r / S r ) = 0 . 7 1 4 0 (
8 7 8 6 0
8 7 8 6 S r / S r ) = 0 . 7 2 1 1 c r u s t
p r e s e n t d a y r o c k w i t h
( S r / S r ) = 0 . 7 0 3 4 (
8 7 8 6 0
8 7 8 6 S r / S r ) = 0 . 7 0 4 5 m a n t l e
r o c k f o r m s f r o m c r u s t a t 1 . 0 M a
r o c k f o r m s f r o m m a n t l e a t 1 . 0 M a
U n d i f f e r e n t i a t e d e a r t h
8 7 8 6 S r / S r = 0 . 6 9 9 a t 4 . 5 M a
8 7 8 6 S r / S r = 0 . 7 0 14 a t 2 . 7 M a
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As crystals form, Rb enriched in melt, eventually can get ultra-enriched (87Sr/86Sr)
Crystals form in magma chamber, Rb stays in melt
magma melts host rock, which has high 87Sr/86Sr
magma chambers with different histories mix prior to eruption
Sr isotopes as tracer of rock origin
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carbonate shells
hydrothermal fluids
sea water
river water87Sr/86Sr = 0.711 87Sr/86Sr = 0.703
87Sr/86Sr = 0.709
87Sr/86Sr = 0.709
Sr in the oceans through time
Sr isotope composition of the oceans is determined by the relative contributions of Sr from river waters and hydrothermal sources
Why is the river Sr isotope
value the highest? Why is the hydrothermal Sr isotope
value the lowest? Why is carbonate recrystallization Sr
isotope value equal to that of seawater?
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Controls on seawater Sr isotopic composition
Seawater Sr Isotopic Curve (as measured on old and young carbonates)
mountain- building
hydrothermal activity
Himalayan uplift
Sr flux rate
Sr isotope ratio
Sr in the oceans through time
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Elemental- and isotopic mixtures
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Binary mixtures
(X)M = (X)AfA + (X)B(1-fA)
fB = 1 - fA
fA = A / (A + B)
−×
+
×
=
M
BA
BM
AA
AM SrSrf
SrSr
SrSrf
SrSr
SrSr )1(86
87
86
87
86
87
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Component A Component B
Sr 100 ppm 500 ppm 87Sr/86Sr 0.800 0.700
G. Faure, 1977, 2005
Binary mixtures
−×
+
×
=
M
BA
BM
AA
AM SrSrf
SrSr
SrSrf
SrSr
SrSr )1(86
87
86
87
86
87
Briquet & Lancelot 1979
(X)M = (X)AfA + (X)B(1-fA)
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Water mixing in estuaries
Chester Marine Geochemistry
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DePaolo & Wasserburg (1979)
Models for crustal contamination
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AFC - process
DePaolo (1981)
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K- metasomatism?
Sr isotopic fingerprinting
Saldenburg granite
Diorite
1 cm
drill holes
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Siebel et al. (2005) Chem Geol 222
Saldenburg granite
Diorite
Sr isotope fingerprinting
1 cm
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Sr isotope fingerprinting
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Isochron or mixing line?
“Redwitzite”
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Si (pfu)8
0.4
0.5
0.6
0.7
0.8
7.5 7.0 6.5
Mg/
Mg+
Fe Magnesio-Hornblende
Ferro-Actinolite
Actinolite
Actin
oliti
cH
ornb
lend
e
Ferro-ActinoliticHornblende
Ferro-Hornblende
Sample R2B
“Redwitzites”: amphibole composition
Siebel et al. (1998) Geology 26
pyx
amp
pyx
bi
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“Redwitzites”: 40Ar-39Ar geochronology
37Ar/39Ar ~ Ca/K 40Ar/39Ar ~ age
Siebel et al. (1998) Geology 26
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White: Geochemistry Lec. 31
Source contamination vs. crustal contamination
Magaritz et al. (1978) EPSL 40: 220-230 James (1981) J. Geol Soc Lond 141:823-830