tectonic heat flow modelling for basin maturation: method .... vanwees...tectonic heat flow...
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Tectonic heat flow modelling for basin maturation: method and applications
J.D. van Wees1,2,
R. Abdul-Fattah1, D. Bonte1,2,
H. Kombrink1, H. Verweij1, F. van Bergen, P. David
F. Beekman2, S. Cloetingh2
2Vrije Universiteit Amsterdam 1TNO
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Content
• Definition of tectonic heat flow
• Workflow
• Added value of tectonic heat flow
• Tectonic models for the Netherlands
• West Netherlands Basin
• Netherlands Antilles
• Terschelling Basin
• Variscan Foreland evolution
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shale k=1.7
sandstone k=2.5
salt k=6
Temperature (T) �
Dep
th (z) �
PD heat flow
q=60
q=80
q=40
q=30
Best fit
Heat flow (q) relates to the temperature
gradient. Present day (PD) Temperature data
(■) in wells can be directly related to (q)
kqdz
dT/=
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tectonic heat flow is calculated from the temperature gradient in the top of the numerical kinematic models, which predict temperature effects of lithosphere deformation.
The 1D McKenzie Model (1978) is a classic for continental lithosphere extension (rifting)
crust
mantle
β =Li/Le
McKenzie model: lithosphere (Li) is instantaneously
thinned by factor β
Li
Le
Temperature (T) �
Dep
th (z) �
120 km
t=100My
t=0My
t=10My
t=30My
t=300My
1330 C
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Tectonics:Lithosphere extension –
Predicted Mass surplus
Sediment record:Burial history-observed mass deficit
Tectonic Subsidence Model (δ δ δ δ = 1.47)
0
200
400
600
800
1000
1200
1400
1600
050100150200
Age [Ma]
Air
lo
ad
ed
te
cto
nic
su
bs
ide
nc
e [
m]
Observed
Model
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For the McKenzie model a very simple analytical solution for the heat flow exist
(McKenzie, 1978)
Heat flow McKenzie Model (for various ββββ -values)
0
20
40
60
80
100
120
020406080100
Age[MA]
Heat
Flo
w [
mW
m-2
]
1.25
1.5
2
3
120 km
McKenzie heat flow
No Good:
•No crustal heat production•No sediment infill
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Heat Flow Model, stretching (β=1.44)
Basement Heat Flow ( Heat production, ββββ=1.44)
45
50
55
60
65
70
75
050100150200
Age[Ma]
He
at
Flo
w [
mW
m-2
]
no sediments
sediments
synrift
Water filled
Sediment filled
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Van Wees and Beekman, 2000 sed
crust
crust
mantle
1/β
Lith
osp
heric
thick
ness
Norm
al geo
therm
dT/dz
stretched
geo
therm
dT/dz
Tectonic
Subsidence
curve
Subsidence Inversion
– tectonic heat flow
Lithosphere
Parameters
Inverted
Tectonic model
TECTONICHEAT FLOW
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Experimental design
SUB
SUBmin, PWDmin
SUBmax, PWDmax
SUBmax, PWDmin
SUBmin, PWDmax
PWDSample, interpolate from
Experimental nodes
Tectonic
Subsidence
curve
Subsidence Inversion
– tectonic heat flow
Lithosphere
Parameters
Inverted
Tectonic model
TECTONICHEAT FLOW
Uncertainty
Tectonic Subsidence
(PWD/erosion)
Heat flow Uncertainty
Uncertainty
Lithosphere
Parameters
(crust/lith)
Experimental designalternative
Inverted
Tectonic models
End-members
UNCERTAINTY TECTONIC
HEAT FLOW
MC sampling
Van Wees et al., 2008
Marine and Petroleum Geology
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Calibration to Ro – PD temperatures – sensitivity analysis
Tectonic
Subsidence
curve
Subsidence Inversion
– tectonic heat flow
Lithosphere
Parameters
Inverted
Tectonic model
TECTONICHEAT FLOW
Uncertainty
Tectonic Subsidence
(PWD/erosion)
Heat flow Uncertainty
Uncertainty
Lithosphere
Parameters
(crust/lith)
Experimental designalternative
Inverted
Tectonic models
End-members
UNCERTAINTY TECTONIC
HEAT FLOW
MC sampling
UncertaintyMaturation
Maturation Uncertainty
Uncertainty
Sedimentary
Thermal properties
MC sampling
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West Netherlands Basin – WAS-2
A priori Uncertainty
•Lithospheric thickness 90-130 km
•Erosion during Late Cretaceous Inversion 500-1500 m
•Porosity depth curves ���� sediment conductivity
Calibration
•Ro depth trend
•PD temperature gradient-
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Subsidence NWB
0
200
400
600
800
1000
1200
050100150200250300350
Age [Ma]
Tecto
nic
su
bs [
m]
data
model
56
50
62
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800+-300 m
EROSION
117+-10km
Lithosphere
thickness
1500
2000
2500
3000
3500
0.2 0.4 0.6 0.8 1 1.2 1.4
Ro [%]
De
pth
[m
]
was-32-
observed
Model
B
0
500
1000
1500
2000
2500
3000
3500
0 50 100 150Temperature[C]
De
pth
[m
]
was-32 -observed
Model
A
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-0.875
Lithospheric thickness [m]
PD
Tem
per
ature
[C
]
Porosity-depth / subsidence 1.7 Ma [m]
PD
Tem
per
ature
[C
]
-0.215
Lithospheric Thickness
Porosity-depth relationship
Sensitivity
Tornado-plot
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• 3D Basin Modeling: How to predict heat flow away from wells?
well
Best fit q=30
q=30?Use linear
extrapolation?
Added value of tectonic heat flow modeling
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70&80s wells, NO HC
SHALLOW WATER, 28 mW
DEEP WATER , 38 mW
Possibly HC
SL
OW
FA
ST
Heat F
low
[mW
m-2
]
Age [Ma]
Netherlands Antilles
Van Wees et al., 2008 – Marine and Petroleum Geology
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• Basin Modeling: How to find heat flow in the past
Age (Ma)
Hea
t F
low
�
Typical start:
Flat heat flow through timeusing the same as PD heat flow
Present day (PD) heat flow
Added value of tectonic heat flow modeling
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• Basin Modeling: How to find better heat flow in the past
Modified to fit Ro
Age (Ma)
Hea
t F
low
�
Added value of tectonic heat flow modeling
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Seismic tomography
demonstrates mantle plumes acting as heat advection channels
in the deep lithosphere
Goes et al., 2000
Ritter et al., 2001
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Extension models – melts and underplates can arise from hot mantle (plumes) which result in accentuated heat advection and heat flow, relative to default extension
http://www.mantleplumes.org/
Crust
Mantle
Norm
al geo
therm
dT/dz
stretched
geo
therm
dT/dz
Underplate
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β=1.5
Lith
osp
heric th
ickness
No
rmal g
eoth
erm
dT/dz
stretched
geo
therm
dT/dz
Crust
Mantle
dT/dz
Ho
t m
antl
e p
lum
eH
ot
man
tle
plu
me
stretched
geo
therm
uniform two-layered
δ=1.5
β=3
Van Wees et al., 2000- – Marine and Petroleum Geology Ziegler et al., 1998 - Tectonophysics
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Sirt Basin
Abadi et al., 2008 –
AAPG Bulletin
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0
500
1000
1500
020406080100
Age [Ma]
Tecto
nic
subs [m
]data
model
synrift
synrift
EAST SIRT- Agedabia WEST SIRT- Hun
0
500
1000
1500
020406080100Age [Ma]
Te
cto
nic
su
bs
[m
]
data
model
synrift
underplating
65
45
55
65
45
55
1500
2000
2500
3000
3500
4000
4500
5000
0.2 0.4 0.6 0.8 1 1.2 1.4 1.6 1.8 2
Ro [%]
Dep
th [
m]
Agedabia-obs
Agedabia-model
HUN-obs
HUN-model
HUN
Agedabia
0
500
1000
1500
2000
2500
3000
3500
4000
4500
0 50 100 150
Temperature [C]
De
pth
[m
]
BHT 22/km
BHT 25/km
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Van Wees et al., 2008 – Marine and Petroleum Geology
0
200
400
600
800
1000
1200
1400
0100200300
Age [Ma]
Tecto
nic
su
bsid
en
ce [m
]
observed
modelled
45
47
49
51
53
55
57
59
61
63
65
Basem
ent h
eat fl
ow
[m
W/m
2]
default heat
flowelevated
West Netherlands
Basinβ=1.5
Lith
osp
heric th
ickn
ess
No
rmal g
eoth
erm
dT/dz
stretched
geo
therm
dT/dz
Crust
Mantle
dT/dz
Ho
t m
antl
e p
lum
eH
ot
man
tle
plu
me
stretched
geo
therm
uniform two-layered
δ=1.5
β=3
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Model building:Boundary conditions
-1600
-1400
-1200
-1000
-800
-600
-400
-200
0
-320 -270 -220 -170 -120 -70 -20
Age [Ma]
Te
cto
nic
su
bs
ide
nc
e [
m]
Tectonic Sub Tectonic Model
55
58
61
64
67
70
Basem
en
t h
eat
flo
w [
mW
/m2]
Calibrated Heat Flow
0.981.011.060.951.0411.111.140.89
-1600
-1400
-1200
-1000
-800
-600
-400
-200
0
-320 -270 -220 -170 -120 -70 -20
Age [Ma]
Te
cto
nic
su
bs
ide
nc
e [
m]
Tectonic Sub Tectonic Model
55
58
61
64
67
70
Basem
en
t h
eat
flo
w [
mW
/m2]
Calibrated Heat Flow
0.981.011.060.951.0411.111.140.89
Basal heat flow historyreconstructed from tectonicmodelling (Petroprob) (Rader Abdul Fattah
et al 2008)
33 heat flow maps
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Willingshofer and Cloetingh, Tectonics 22, 2003
Ziegler et al., 1998
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Carboniferous –Netherlands (1)
Kombrink et al., 2008 (Basin Research)
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Carboniferous –Netherlands (2)
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Carboniferous –Netherlands (4)
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Conclusions
• Tectonic heat flow models aid in predicting heat flow for basin
modelling beyond well control
• Mature basins - Heat flow through time
• Frontier basins – spatial variability
• Tectonic heat flow models should include effects of crustal heat
production and sediment infill/erosion
• The Netherlands
• Average heat flow values today
• Considerable variation through time:
• Elevated at mantle plume/underplating phase
• Depressed during foreland formation