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ISSN: 2168-9873

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Research - (2019) Volume 8, Issue 1

Thermo-mechanical model of the mantle wedge between the base of the overlying Scythian lithospheric plate and the upper surface of the Black Sea micro-plate subducting under the Scythian one with a velocity V at an angle β is obtained for the infinite Prandtl number fluid as a solution of non-dimensional 2D hydrodynamic equations in the Boussinesq approximation. For both Newtonian and non-Newtonian rheology cases 2D thermal viscous dissipationdriven convection mechanism in the mantle wedge above the Black Sea micro-plate subducting under the Crimea peninsula is modelled numerically. The effects of 410 km and 660 km phase transitions are taken into account. In the case of Newtonian rheology, the upwelling convective flow transporting heat to the Earth’s surface locates at far greater distance from the trench than they observed 2D heat flux anomaly. In the case of non-Newtonian rheology, the upwelling convective flow transporting heat to the Earth’s surface locates at twice greater distance from the trench than they observed 2D heat flux anomaly, the velocity in the convective vortices being over ∼10 m per year.

2D hydrodynamic equations; Boussinesq approximation; Runge-Kutta method; Newtonian; Non-Newtonian rheology cases; Thermal convection; Subduction angle and velocity; Hydrocarbons transport

Interaction of the lithospheric plates in the Crimea-Caucasus
region leads to thrusting of the Black Sea micro-plate under the Crimea
peninsula (under the Scythian plate) [1]. As a consequence, the seismic
focal plane is formed along which the Crimea ascends as the result of
seismic jerks. The velocities of vertical uplift of the Crimea mountains
and sinking of the near-Crimean area of the Black Sea micro-plate equal
to ∼4 mm per year and ∼10 mm per year respectively. Mountainous
Crimea is a folded fault region being a part of the Alps-Himalaya-
Indonesia belt [2-5]. The velocity of subduction of the Black Sea microplate
under the Crimea peninsula remains unknown. According to
[3-5] two types of dissipation-driven small-scale thermal convection
in the mantle wedge are possible, viz. 3D finger-like convective jets,
raising to volcanic chain, and 2D transversal Karig vortices, aligned
perpendicularly to subduction. These two types of convection are
shown to be spatially separated due to the pressure and temperature
dependence of mantle effective viscosity, the Karig vortices, if any of
them formed, being located behind the volcanic arc [6]. Despite the
firmly established localization of both seismic focal plane and the deepsea
trench parallel to the southern shore of Crimea there are no definite
conclusions concerning the velocity of subduction of the Black Sea
micro-plate. It is not completely clear if volcanism played a substantial
role in forming Mountainous Crimea or the mountains are of a purely
thrust-and-fold origin. Nimelulayeva [1] indicates the contradictory
statements on the Crimean volcanism to have been published,
however in **Figure 1** in Nimelulayeva [1] the volcanic eruption in
the Mountainous Crimea is depicted. The abovementioned picture
is reproduced here in **Figure 1** with the convective vortices drawn
additionally. It is worth assuming the two heat flux anomaly maxima
observed in the south of the Crimea peninsula [1,7] owe their origin
to respectively 3D and 2D upward convective heat transfer from the mantle wedge to the Earth’s surface (**Figure 1**). The latter 2D maximum
located in the rear of the Mountainous Crimea is much greater as
compared to the former 3D maximum located in the Mountainous
Crimea. The 2D heat flux anomaly maximum obviously is associated
with the 2D upward convective flow in the mantle wedge. Numerical
modelling of 2D mantle wedge thermal convection occurring in the
form of the Karig vortices and presumably transporting heat to the
Earth’s surface in the rear of the Mountainous Crimea allows to judge
about the mean velocity of subduction of the Black Sea micro-plate
under the Crimea peninsula as well as about the rheological mantle
parameters. Horizontal extent of the 2D heat flux anomaly in the
rear of the Mountainous Crimea is shown to correspond to the mean
subduction velocity ∼45 mm per year for the observed subduction
angle ~15°. Numerical convection models accounting for the effects
of phase transitions as well as the pressure, temperature and viscous
stresses viscosity dependence fit in well with the heat flux observation
data in the case of non-Newtonian mantle rheology at the mantle
wedge water concentration ~3 × 10^{-1} weight%.

**Figure 1: **(1) Schematic cross section of the region of subduction of the Black Sea micro-plate under the Crimea peninsula (Scythian lithospheric plate) C_{1} and
C_{2} are the zones of 3D and 2D convective flows ascending to the heat flux q maxima, the whirls under C_{2} are the 2D Karig convective flows. (2) Heat flux q in the
south of Crimea. (3) The Black Sea micro-plate subducting under the Crimea peninsula and the seismic focal plane shown by the dotted line [1].

Thermo-mechanical model of the mantle wedge between the base of the overlying Scythian lithospheric plate and the upper surface of the Black Sea micro-plate subducting under the Scythian one with a velocity V at an angle β is obtained for the infinite Prandtl number fluid as a solution of non-dimensional 2D hydrodynamic equations in the Boussinesq approximation:

(1)

(2)

For the stream function ψ and temperature T. Here η is non-dimensional
dynamic viscosity, ∂ and indices denote partial derivatives with respect
to coordinates x (horizontal), z (vertical) and time t, Δ is the Laplace
operator, Г^{(410)} and Г^{(660)} are volume ratios of the heavy phase at the 410
km and 660 km phase boundaries, the velocity components *V _{x}* and

(3)

and non-dimensional Rayleigh number Ra, phase Ra (410), Ra (660) and dissipative number Di are defined as follows

(4)

Where a =3.10^{-5} K^{-1} is thermal expansion coefficient, ρ=3.3 g × cm^{-3} is
the density, g is gravity acceleration, *c _{p}*=1.210

(5)

Where for “wet” olivine A=5.3 × 10^{15} s^{-1}, *m*=2.5, the grain size *h*=10^{-1} -10
mm, Burgers vector is b*=5 × 10^{-8} cm [10], activation energy is E*=240
kJ × mol^{-1}, activation volume *V**=5 × 10^{3} mm^{3} × mol^{-1} is activation
volume, = 300 GPa is normalizing factor of the shear modulus, *R* is
universal gas constant. Under grain size *h*=1.6 mm, ç = 10^{18} Pa × s and
abovementioned values of constants non-dimensional viscosity also
denoted η is:

(6)

Where T is non-dimensional temperature, non-dimensional z
normalized by d is pointing upwards from the MTZ base and x is
pointing against subduction along the MTZ base. The aspect ratio of
the model domain is 1:3.7 thus the subduction angle being β=15° if
subduction is assumed to take place along the model domain diagonal.
Non-dimensional subduction velocity V=45 mm.yr^{-1} normalized by
(d^{-1}_{x}c) equals V=0.938 × 10^{3}, i.e. non-dimensional velocity components
of subducting Black Sea micro-plate are V_{x}= -0.898 × 10^{3} and V_{z}=-0.268
× 10^{3}.

To check as to how the estimate of velocity of subduction of the Black Sea micro-plate is sensitive to the accepted linear rheological law here, we make extra computations for non-Newtonian rheology, in which case the viscosity formulae (5)-(6) are rewritten as

(7)

Where according to Trubutsyn [11] for “wet” olivine n=3, r=1.2, m=0,
E*=480 kJ.mol^{-1}, V*=11 × 10^{3} mm^{3}.mol^{-1}, A=10^{2} с^{-1} × (MPa)^{-n}, C_{w}>10^{-3} for “wet” olivine is the weight water concentration (in%%). It should
be noted the constants in equation 7 vary considerably in the papers
referred to by Trubutsyn [11] and heretofore we gave averaged values
of constants.

At C_{w}=10^{-3} on accounting for

(8)

non-dimensional viscosity is

(9)

Following Trubutsyn [12] we assume the phase functions Г* ^{(l)}* as

(10)

Where the signs are changed as z-axis is pointing upwards, z^{(l)}(T) is
the depth of the l-th phase transition (l=410, 660), z_{0}^{(l)} and T_{0}^{(l)} are
the averaged depth and temperature of the *l*-th phase transition, ^{(410})=3 MPa×K^{-1} and γ^{(660)}=-3 MPa×K^{-1} are the slopes of the phase equilibrium curves, w^{(l)} is the characteristic thickness of the l-th phase
transition, T0(410)=1800o K, *T _{0}*

(11)

Where from it is clear the phase transition with facilitates
convection (at l=410), while the phase transition with γ^{(l)}<0 hinders
convection (at l=660). In non-dimensional form z_{0}^{(410)}=0.38, z_{0}^{(660)}=0,
w^{(l)}=0.05, γ^{(410)}=2.5×10^{9}, T_{0}^{(410)}=0.92, T_{0}^{(660)}=1, and in (1):

(12)

Equation 1 and equation 2 are solved for the isothermal horizontal and insolated vertical boundaries regarded no-slip impenetrable
ones except for the “windows” for in- and outgoing subducting
plate, where the plate velocity is specified. Vertical boundary distant
from subduction zone is assumed penetrable at right angle, the latter
boundary condition appears not too imposing in the case of very flat
subduction. Q in equation 2 is non-zero in the continental and oceanic
crust 40 and 7 km thick. Initial vertical boundaries temperature is
calculated for the half-space cooling model for 109 yr and 108 yr for
Scythian (continental) and Black Sea (oceanic) plates respectively. It
is convenient to express dimensionless ^{2}_{ik} in equation 2 through the
stream-function Ψ as in equation 8:

Assuming the second (more remote from the trench) heat flux q
maximum in **Figure 1** appears above the convective flow, ascending to *C*_{2} point in **Figure 1**, and the convection cell dimension is equal to the
two adjacent q minima separation (i.e. the q minima are located above
the descending convective flows) we can estimate the convection cell
dimension as ~250 km. To preliminarily access the mean velocity of
subduction of the Black Sea micro-plate the coordinate x dependence
of the growth rate γ_{1}(x) of transversal convective rolls for the constant
viscosity fluid model can be allowed for. In such the model the average
temperature and pressure viscosity dependence is accounted for in an
averaged manner, the factor describing the temperature- and pressure
viscosity dependence being equal to its mean value [3].

Analytical formulae by Gavrilov [3] yield γ1(x) shown in **Figure 2** for the subduction angle β=15° convection cell dimension ~250 km
and subduction velocities V given in **Figure 2** in mm per year.

**Figure 2: **Growth rate 1(x) of convective instability vs. horizontal distance x for subduction velocities V in mm per year. In the zone x_{1}<x<x_{2} approximately 250 km
long single 2D convection cell with (x)>0 is aroused at V=40.5 mm × yr^{-1} in the zone of heat flux maximum.

It should be noted the growth rates γ_{1}(x) are viscosity independent
as convection is driven by viscous heat release (which is directly
proportional to viscosity), while, on the other hand, the greater is
the viscosity the more difficult is to arouse the convection. **Figure 2** clearly demonstrates the convective zone with γ_{1}(x)>0 amounts to
(*x _{2} – x_{1}*)=250 km (i.e. the single convective cell of ~250 size is actually
aroused) at V=40.5 mm per year, the latter value being a preliminary
estimate of the mean subduction velocity. The γ

To compute more accurate consistent model of small-scale
convection in the mantle wedge between the overriding Scythian
plate and subducting Black Sea micro-plate it is necessary from the
computational point of view first to specify in equation (1)-(2) vanishing
non-dimensional numbers Ra→0, Di=0, i.e. to ignore convection and
viscous dissipation. This approach is applied as convection with Ra
and Di (4) passes through very vigorous stages, and the time steps in
integrating equation (1)-(2) become too small thus making it difficult
to model the thermal structure of the plates. Solving equation (1)-(2)
by the finite element method in space on the grid 104×104 and the 3-rd
order Runge-Kutta method in time one obtains for Ra→0, Di=0 and V=45
mm a year non-dimensional quasi steady-state Ψ and T shown in **Figure
3**, where the streamlines are depicted with the step 0.25 and the isotherms
with an interval 0.05. Subducting plate was considered rigid, while the
viscosity at the zone of plate’s friction (at temperatures below 1200 K)
was reduced by 2 orders of magnitude as compared to equation 5. The
latter viscosity reduction at the plates contact zone accounts for lubrication
effected by deposits partially entrained by the subducting plate.

Such a lubrication prevents the overriding Scythian plate from
gluing to the subducting one [5]. It is worth noting the isotherm T=0.15
in **Figures 3a** and **3c** approximately corresponding to the Earth’s
surface is depressed at subduction zone by ~7 km which is of the order
of a typical trench depth. **Figure 3** shows the results of computation
for formulae equation (7)-(9) for non-Newtonian rheology case for the
water content C_{w}=10^{-3} weight%% (**Figures 3a** and **3b**) and C_{w}=3 × 10^{-1} weight%% (**Figures 3c** and **3d**). The velocity V=45 mm per year is chosen
as resulting in the best convective zone size fitting in with the observed
heat flux (positive and negative) anomaly size at the point C_{2} in **Figure
1**, i.e. in the rear of the Mountainous Crimea. The Black Sea micro-plate
subducting with a given velocity *V* is considered rigid and is shown in **Figures 3b** and **3d** by the equidistant diagonal streamlines. The induced
mantle wedge flow above the subducting plate is seen to occur in the
form of a single vortex at C_{w}=10^{-3} weight%% (**Figure 3b**) and in the form
of the 2 vortices (located one above another) at C_{w}=3 × 10^{-1} weight%%
(**Figure 3d**), the latter 2 vortices being considerably compressed in the
vertical direction and the upper one (with Ψ >0) revolves clockwise while the lower one (with Ψ< 0) revolves counterclockwise (**Figures 3b** and **3d**). Micro-whirls ~10^{2} km great are formed between the counterflows
inside the upper induced flow obviously due to the tangential
discontinuity instability (Kelvin-Helmholtz instability).

**Figure 3:** Quasi steady-state non-dimensional stream-function and temperature distributions in the zone of subduction of the Black Sea micro-plate under the
Scythian plate with no effects of dissipative heating and convection taken into account for non-Newtonian rheology: (a and b) for the water content Cw=10^{-3} weight
%% and (c and d) for the water content C_{w}=3 × 10^{-1} weight %%. Parallel equidistant streamlines represent subducting Black Sea micro-plate, the strealines above
correspond to the mantle wedge flow induced by subduction.

Assuming Ra=5.55 × 10^{8} and Di=0.165, i.e. switching dissipation
and convection on, and taking into account the effects of phase
transitions, from equation 1– equation 2 the convection is found not to
arouse in the non-Newtonian rheology case at C_{w}= 10^{-3} weight%%. At
C_{w}=3 × 10^{-1} weight%% the 2 induced mantle flows in the mantle wedge
are destroyed during the time interval ~ 0.6 × 10^{-6} (in dimensional
form ~ 0.1 Myr) by the convective vortices shown in **Figure 4** with the
streamlines depicted with the interval 4 × 10^{4}.

**Figure 4: **Quasi steady-state stream-function in the mantle wedge with the effects of dissipative heating and convective instability for the case of non-Newtonian
rheology and the water content C_{w}=3 × 10^{-1} weight %%. Arrow (c) shows ascending convective flow transporting mantle hydrocarbons to the Earth’s surface at
the point C_{2} in Figure 1.

These convective vortices are seen actually to correspond to a single
convection cell aroused at subduction velocity V=45 mm per year. The
latter convection cell dimension is of the order of ~300 km, i.e. is very close
to the observed minima q separation under the C_{2} point in **Figure 1**.

Thus the for the non-Newtonian mantle wedge rheology case
with the viscosity reduced by 3 orders of magnitude as compared to
equation 7–equation 9 the computation shows the convection in the
mantle wedge to occur at C_{w}=3×10^{-1} weight%% in the form of two micro
vortices at V=45 mm per year. Convection of this type can provide
abnormal 2D heat flux q observed in the rear of the Mountainous
Crimea. Alternatively, the water content can be not that greatly
increased but the constant A in equation 7 might have been an order
(or so) of magnitude greater. Considerable velocity in convective vortices
in **Figure 4** is due to the local viscous stresses increase resulting in the
drop in viscosity in convective zone. It is worth noting the mantle wedge
dissipation-driven convection in the form of transversal rolls as in **Figure 4** is characteristic of very small subduction angles the convection of this type
being absent already at subduction angle β=30° [13]. At the subduction
angle under consideration here, β=15°, the convective transversal rolls
do not appear at V<4 cm × yr^{-1}. Arrow *(c)* above the boundaries of the
oppositely revolving convective vortices in **Figure 4** indicate possible
direction of transport of non-organic mantle hydrocarbons to the Earth’s
surface. Computations for Newtonian mantle rheology with the viscosity
equation 5-equation 6 shows the transversal rolls to be aroused at far
greater distance from the trench than the observed 2D heat flux anomaly.
Thus, the model constructed here favors the non-Newtonian mantle
wedge rheology as better fitting in with the observed heat flux anomaly
localization. It should be noted that numerous thermo-mechanical mantle
models in the zones of subduction (see, e.g. [4,5] and the vast number of
references there) showed convection in the form of transversal rolls never
to occurred as the models with extremely small subduction angle and
sufficiently great subduction velocity were not investigated.

The size of the cell of 2D mantle wedge dissipation-driven
convection in the case of the realistic non-Newtonian rheology equals
~300 km at the subduction velocity 45 mm×yr^{-1}, in which case a single
convection cell is aroused. This explains the formation and horizontal
extent of the only 2D heat flux anomaly observed in the rear of the
Mountainous Crimea. The water content enough for the 2D convection
be aroused is ~3×10^{-1} weight%%, or, alternatively, it is, say, ~3 × 10^{-2} weight%%, but the constant A in the rheological law is an or[der of
magnitude greater than generally accepted. The non-Newtonian model
convection cell locates twice further from the trench than the 2D heat
flux anomaly is observed, this discrepancy being even greater in the
case of Newtonian rheology. However linear onset of convection model
shows the position of 2D convection cell to nearly coincide with the
observed 2D heat flux anomaly for constant viscosity fluid model for
subduction velocity 40 mm per year. The velocity in convective vortices
in the non-Newtonian rheology case is ~10 m per year which may be
enough to provide upward transport of mantle wedge hydrocarbons to
the Earth’s surface.

The authors would like to express sincere thanks to Dr. Joseph Abraham for his help in publishing the paper.

- Nimelulayeva G. Peculiarities of the influence of natural factors and their bearing on formation of the land-slide processes in Crimea. Culture of the Near Black Sea People. 2006;83:110-113.
- Yudin VV. Crimea geology on the geodynamical basis, Simpheropol. 2001;2:1.
- Gavrilov SV. Investigation of the mechanism of island arc formation mechanism and the back-arc lithosphere spreading of the lithosphere. Geophysical Researches. 2014;5:35-43.
- Gerya TV, Connolly JAD, Yuen DA, Gorczyk W, Capel P. Seismic implications of mantle wedge plumes. Phys Earth Planet Inter. 2006;156:59-74.
- Gerya T. Future directions in subduction modeling. J Geodyn. 2011;52:344-378.
- Gavrilov SV, Kharitonov AL. Subduction velocity of the Russian plate under the Siberian one at Paleozoic: A constraint based on the mantle wedge convection model and the oil and gasbearing zones distribution in Western Siberia. Modern Science. 2016;16:155-160.
- Smirnov-Ya B. The map of heat flux at the territory of the USSR and adjacent regions. 1980.
- Billen M, Hirth G. Newtonian versus non-Newtonian upper mantle viscosity: Implications for subduction initiation. Geophys Res Lett. 2005;p:32.
- Zharkov VN. Physics of the Earth’s Interiors. Moscow, Science and Education. 2012.
- Zharkov VN. Geophysical researches of the planets and satellites. Moscow, Joint Institute of Physics of the Earth RAS. 2013;p:102.
- Trubutsyn VP. Rheology of the mantle and tectonics of oceanic lithosphere plates. Izv Phys Solid Earth. 2012;6:3-22.
- Trubutsyn VP. Trubitsyn AP Numerical model of formation of the set of lithospheric plates and their penetration through the 660 km boundary. Izv Phys Solid Earth. 2014;6:138-147.
- Gavrilov SV, Abbott DH. Thermo-mechanical model of heat and masstransfer in the vicinity of subduction zone. Izv Phys Solid Earth. 1999;35:967-976.

**Citation:** Kharitonov AL, Gavrilov SV (2019) The Comparison of Newtonian and Non-Newtonian Rheology Cases of the Solution of 2D Hydrodynamic Equations in the Boussinesq Approximation: A Mechanism of Upwelling Convective Flow Transporting Hydrocarbons. J Appl Mech Eng 7: 314. doi: 10.35248/2168-9873.19.8.314

**Received Date:**
Aug 29, 2018 / **Accepted Date:**
Dec 31, 2018 / **Published Date:**
Jan 04, 2019

**Copyright:** © 2019 Kharitonov AL, et al. This is an open access article distributed under the term of the Creative Commons Attribution License, which permits unrestricted use, distribution, and reproduction in any medium, provided the original author and source are credited. This is an open access article distributed under the terms of the Creative Commons Attribution License, which permits unrestricted use, distribution, and reproduction in any medium, provided the original work is properly cited.