CHI GuoXiang

池国祥

Department of Geology，University of Regina，Regina，Saskatchewan S4S 0A2，Canada

加拿大里贾纳大学地质系

1 Introduction

The formation of hydrothermal mineral deposits requires circulation of large amounts of fluids through the sites of mineralization. A comprehensive mineralization model not only explains the chemical processes of mineralization，including the sources of fluids and metals，the solubility of metals and their speciation in hydrothermal solutions，and the ore deposition mechanisms，but also addresses the physical processes of fluid flow，including the driving forces，flow direction，velocity，and duration (Norton and Cathles，1979;Cathles，1981;Garven and Raffensperger，1997;Cathles and Adams，2005;Cox，2005;Chi and Xue，2011a;Ingebritsen and Appold，2012;Zhao et al.，2012). While the chemical processes can be evaluated with many different geochemical tools，the assessment of the physical processes relies heavily on numerical modeling of fluid flow (e.g.，Cathles and Smith，1983;Garven and Freeze，1984a，b;Bethke，1986;Sanford，1994;Raffensperger and Garven，1995;Chi and Savard，1998;Appold and Garven，2000;Oliver et al.，2006;Yang et al.，2006;Zhang et al.，2006;Xue et al.，2010;Zhao et al.，2010，2012;Cui et al.，2012). Unlike modern groundwater flow models，which may be calibrated with present-day observations，the numerical models of paleo-fluid flow systems related to mineralization are difficult to verify. As a result，multiple fluid flow models may be proposed for a given mineralization system，even though only one of them may be correct. Although no single method may solve this problem，fluid inclusion study is probably one of the best to provide important constraints on paleo-fluid flow models related to mineralization，which is the main topic of this paper.

Fluid inclusions have played an important role in the studies of mineral deposits (e.g.，Roedder，1984;Roedder and Bodnar，1997;Wilkinson，2001;Chi et al.，2003;Lu et al.，2004;Chi and Lai，2009). This is in part reflected by the large number of papers with a component of fluid inclusion studies published in journals specialized in mineral deposits geology. For example，the percentage of papers containing fluid inclusion studies in Economic Geology has increased from 7% in 1970 to 21% in 2010，with a peak of 27% in 1995 and 2000 (Fig.1).The contributions that fluid inclusions have made to studies of mineral deposits include providing 1)information about the compositions of the mineralizing fluids and the physicochemical conditions of mineralization;2) key evidence for certain mineralization processes，especially fluid mixing and fluid phase separation; 3 ) supporting evidence for mineral deposit classification;and 4)constraints on hydrodynamic models of mineralization (Chi and Lai，2009). Although fluid inclusion data have been used in establishing fluid flow models of mineralization， the contributions of fluid inclusions for hydrodynamic studies of mineralization have not been systematically examined in the literature. This paper will elaborate on the fundamental relationships between fluid inclusion and hydrodynamic studies，review various developments that have been made so far，and discusses research directions in the future.

Fig. 1 Percentage of papers containing fluid inclusion studies in Economic Geology in selected years

2 Fundamental relationships between fluid inclusion and hydrodynamic studies

Fluid flow in porous media is generally governed by Darcy’s law，which describes fluid flow rate as a function of hydraulic head gradient and hydraulic conductivity of the media. It has been shown that hydraulic head is related to fluid pressure and elevation，and Darcy’s law can be expressed as:

where q is flow rate，k is rock permeability，μ is fluid viscosity，L is distance，and Φ is hydraulic potential (Hubbert，1940)，which is defined as:

Where ρ is fluid density，g is gravity，z is elevation，and P is fluid pressure. Therefore，fluid flow is related to fluid density and fluid pressure.

It has been generally agreed that the formation of hydrothermal ore deposits involves complex，coupled processes including thermal，hydraulic，mechanic，and chemical (THMC)(Ingebritsen and Appold，2012). Geologic fluid flow is always accompanied by heat transfer，which includes heat conduction and heat advection，the latter being directly related to fluid flow velocity. Furthermore， fluid flow systems associated with mineralization are generally accompanied by mineral precipitation or dissolution，which is associated with changes in concentrations of dissolved species， known as reactive mass transport.Therefore，a complete hydrodynamic characterization of a mineralizing fluid flow system consists of determination of four fundamental parameters in space and time，i.e.，fluid pressure(P)，density or specific volume (V)，temperature (T)，and composition (X)，in addition to other important parameters such as permeability.

Remarkably，these four parameters (PVTX)are also what fluid inclusion studies are mainly about. Fluid inclusions represent the only actual samples of the paleo-fluids in mineralizing systems，and can provide unique information about the composition of the fluids (the “X”) through various analytical methods (Roedder，1984;Chi et al.，2003;Lu et al.，2004). One of the most important methods of fluid inclusion studies is called microthermometry，which can provide important constraints on fluid density (the“V”)and temperature(the“T”)，based on the assumption that the fluid inclusions entrapped a homogeneous fluid and have not been subject to volume and compositional changes after entrapment (Roedder，1984;Goldstein and Reynolds，1994;Chi and Lu，2008).Furthermore，fluid pressure (the“P”)can be estimated，under certain conditions，from isochores derived from fluid inclusion microthermometric studies， known as fluid inclusion geobarometer (Roedder and Bodnar，1980).

Fig. 2 A fictional cross-section showing the spatial distribution of fluid pressure (P )， density (V )，temperature (T)and salinity (X)obtained from fluid inclusion studies，at a given time during the formation of a mineral depositSuch a set of PVTX data may be used to “calibrate” the hydrodynamic model of the mineralization system. See the text for more explanation

Thus，the hydrodynamic and fluid inclusion studies of mineralization systems are linked together through a common fundamental interest in fluid pressure，density，temperature and composition. The hydrodynamic characterization of a mineralization system may be conducted through numerical solution of four governing equations，i.e.，fluid flow，heat transfer，rock deformation，and mass transport，which produces a temporal and spatial distribution of fluid pressure，temperature，density and composition. Many different sets of computational results may be obtained using different combinations of driving forces，permeabilities，and initial and boundary conditions，resulting in multiple hydrodynamic models.If we can determine the temporal and spatial distribution of fluid pressure，temperature，density and composition through fluid inclusion studies，as depicted in Fig.2，we may be able to modify the hydrodynamic model to match the computational results with those from fluid inclusion studies. In other words，the numerical models may be“calibrated”. Admittedly，such work is unrealistic at present because it is difficult to assure the contemporaneousness of two fluid inclusions from different localities，and the amount of work involved in obtaining accurate PVTX data in many localities is tremendous. However，through this idealized scenario it is emphasized that fluid inclusion studies can provide important constraints on hydrodynamic models，and such constraints may be improved in the future with the advancement of fluid inclusion analysis techniques.

3 Fluid pressure and pressure regime estimated from fluid inclusions

As discussed above，fluid pressure is an important parameter in characterizing the hydrodynamic system，and it can be estimated from fluid inclusion studies. However，as discussed by Roedder and Bodnar (1980)，it is not straightforward to obtain fluid pressure values from fluid inclusion data. The most common fluid inclusion geobarometers and potential problems associated with them are discussed below. These geobarometers are based on the same principle that the PVTX data of a fluid inclusion can be used to construct an isochore in the T-P space using the equation of state (EOS)of an approximate fluid composition system， and thus if the temperature can be determined， the pressure can be calculated. Significant uncertainties of the isochores can be caused by large discrepancies between EOS by different authors，as compiled in software packages (Brown，1998;Bakker，2003)，and by inaccuracies of the analytical results of the fluid inclusions.

The most common fluid inclusions found in mineralization systems are aqueous inclusions that homogenize into the liquid phase，whose isochores are generally steep in the T (horizontal axis)-P (vertical axis)space (Fig.3a). The fluid pressure(Ph)at the homogenization temperature (Th)is generally much lower than the actual fluid pressure at entrapment (Pt)(Fig.3a). If the trapping temperature (Tt)of fluid inclusion(or the formation temperature of the host mineral)is known from other methods (e.g.，stable isotope geothermometers)，Ptcan be calculated from the isochore (Fig.3a)(e.g.，Chi et al.，2011). If Ttis not known but the thermal gradient and the fluid pressure regime (hydrostatic versus lithostatic;see more details below)are known，the intersection between the isochore and the thermal gradient line may indicate the trapping temperature and pressure (Fig.3b)(e.g. ，Derome et al.，2005). Because of the steep slope of the isochore，a minor error in estimation of trapping temperature can result in a large error in pressure，therefore the isochores of aqueous inclusions are generally not good geobarometers. In the case of Fig.3b，large uncertainties in fluid pressure are also related to the estimation of thermal gradient and fluid pressure regime，as indicated by the large difference in estimated fluid pressure between hydrostatic and lithostatic systems (Fig.3b). Furthermore，the fluid pressure(Ph)at homogenization temperature (Th)may have been significantly underestimated due to inability to detect other volatiles besides water，as illustrated in Fig.3c (Hanor，1980).For fluid inclusions containing daughter minerals，if the melting temperature of the daughter mineral (Ts)is higher than the liquid-vapor homogenization temperature (Th)，the pressure corresponding to this melting temperature (Ps)may provide a minimum estimation of the trapping pressure (Fig.3d)(e.g.，Chi et al.，2011).

Fig.3 Various methods of estimating fluid pressure from fluid inclusion data(a)fluid pressure estimated from isochore of aqueous inclusion in conjunction with an independently determined trapping temperature;(b)fluid pressure estimated from intersection between isochore of aqueous inclusion and the geothermal gradient lines associated with hydrostatic and lithostatic systems;(c)potential underestimation of fluid pressure due to non-detection of volatiles besides water;(d)fluid pressure corresponding to melting temperature of daughter mineral as a minimum estimation of the trapping pressure;(e)relatively gentle isochore of carbonic or petroleum inclusion，producing relatively accurate trapping pressure from independently determined trapping temperature;(f)fluid pressure estimated from intersection between isochores of aqueous and carbonic or petroleum inclusions;(g)fluid pressure estimated from the isochore of carbonic or petroleum inclusion in conjunction with the homogenization temperature of coexisting aqueous inclusion;(h)isochores of vapor and liquid fluid inclusions entrapping two immiscible fluids，with the homogenization temperature and pressure being equal to the trapping temperature and pressure，respectively. Th =homogenization temperature;Tt =trapping temperature;Ts =melting temperature of daughter mineral;Ph =homogenization pressure;Pt =trapping pressure;Ps =fluid pressure corresponding to melting temperature of daughter mineral;aq=aqueous inclusions;isoc=isochore

In contrast to aqueous inclusions，carbonic (CO2，CH4，or CO2+ CH4+ N2)and petroleum inclusions are generally characterized by relatively gentle isochores in the T-P space(Fig.3e)， and make better geobarometers than aqueous inclusions. If the trapping temperature can be determined independently，the fluid pressure can be calculated with relatively small errors. A potential complexity with the carbonic inclusions is that there may be an invisible aqueous phase wetting the inclusion wall (Roedder，1984)，which may reduce the accuracy of the isochores. One practice to minimize such potential errors is to search for relatively large inclusions with acute corners，where an aqueous phase is relatively easy to be seen if present (Chi et al.，2006). It is not uncommon to observe aqueous inclusions together with carbonic or petroleum inclusions，and there are two different ways of using the aqueous inclusions to estimate fluid pressure in conjunction with the carbonic or petroleum inclusions. One is to construct the isochores of the aqueous inclusions and use the intersection with the isochores of the carbonic or petroleum inclusions to represent the trapping pressure (Fig.3f)(Chi et al.，1995)，and the other is to use the homogenization temperature of the aqueous inclusions to represent the trapping temperature and to calculate the fluid pressure accordingly (Fig.3g)(Chi et al.，2000，2005，2008，2011;Chi and Xue，2011b). The first approach is based on the assumption that the aqueous and carbonic (or petroleum)fluids were not in touch (and so not in equilibrium)with each other;such assumption is difficult to ascertain，and may result in an overestimation of fluid pressure because of the underestimation of volatiles in the aqueous inclusions (similar to the situation depicted in Fig.3c). The second approach is based on the assumption that the aqueous and carbonic (or petroleum)fluids were in equilibrium (i.e.，immiscibility)，and so the aqueous fluid was saturated with carbonic (or hydrocarbon)volatiles at entrapment， meaning that the homogenization temperature is equal to the trapping temperature. Such assumption is probably valid in relatively stable sedimentary basins，as in petroleum reservoirs (e.g. ，Aplin et al.，1999)，but may be invalid in more active environments such as orogenic gold systems，where the aqueous fluid may have been physical separated from the carbonic fluid and been purged of the latter during episodic fluid pressure fluctuation，leading to formation of aqueous inclusions undersaturated with carbonic components at entrapment (Robert and Kelly，1987). In such a case，both the trapping pressure and temperature may be underestimated.

In the case of fluid immiscibility，including boiling，theoretically the homogenization temperatures of the fluid inclusions resulting from homogeneous trapping of the two immiscible phases (liquid and vapor)should be identical and should be equal to the trapping temperature，and the fluid pressure estimated from the two isochores should be identical and equal to the trapping pressure as well (Roedder and Bodnar，1980;Roedder，1984)，as illustrated in Fig.3h (e.g.，Chi et al.，1993). In practice，it is relatively difficult to determine the composition and homogenization temperature of the vapor inclusions，thus losing the ideal mutual validation of the paired isochores. In such cases，the homogenization temperature and pressure of the liquid inclusions are taken to represent the trapping temperature and pressure (e.g. ，Chi and Xue，2011b;Chi et al.，2011)，but it is cautioned that these liquid inclusions should be distinguished from those trapping the preimmiscibility homogeneous fluid.

In addition to fluid pressure，the fluid pressure regime also plays an important role in hydrodynamics of mineralization systems. Fluid pressure regime refers to the relationship between fluid pressure and the hydrostatic and lithostatic pressure systems at a given depth. A fluid pressure regime is said to be hydrostatic if fluid pressure is equal to the pressure produced by a column of fresh water above the point of interest，or lithostatic if the fluid pressure is equal to that produced by a column of rock above(Roedder and Bodnar，1980). A fluid pressure regime is hypohydrostatic if fluid pressure is lower than the hydrostatic value，supra-hydrostatic if fluid pressure is between hydrostatic and lithostatic values，and supra-lithostatic if fluid pressure is higher than the lithostatic value. A fluid system is said to be overpressured if fluid pressure is higher than hydrostatic (suprahydrostatic， lithostatic， or supra-lithostatic )， and fluid overpressure or excess pressure refers to the difference between fluid pressure and hydrostatic pressure at a given depth (Bethke，1985;Zhao et al.，1998).

It can be shown that when there is no topographic relief，fluid overpressure is equal to hydraulic potential (Chi and Xue，2011a)，supporting that fluid pressure regime is directly related to fluid flow mechanism. Fluid flow driven by topographic relief and fluid convection driven by density variation are relatively easy to develop when the fluid-pressure system is near hydrostatic;strong fluid overpressure tends to suppress such fluid flow，although it has been shown that fluid convection is still possible in overpressured systems under certain conditions (Zhao et al.，2000). The mechanism of fluid flow related to structural deformation is also related to the fluid-pressure regime. In environments where the ambient fluid pressure is hydrostatic(such as in epithermal mineralization)，fluid pressure may fluctuate between hydrostatic and hypo-hydrostatic values in response to fracturing，and fluid flow may be driven by the suction pump mechanism，whereas in environments in the hydrostatic-lithostatic transition zone (e.g. ， mesothermal mineralization)，fluid pressure may fluctuate between hydrostatic and lithostatic values in response to episodic fracturing(earthquakes)and fluid pressure build up，as explained by the fault valve model (Sibson et al.，1988).

The fluid pressure regime or the exact overpressure value can only be determined if both the fluid pressure and the depth can be independently estimated. However， approximate estimation of the pressure regime can still be made based on fluid pressure，fluid pressure fluctuation，and geologic conditions. In magmatic-hydrothermal systems，lithostatic to supra-lithostatic fluid pressure may be developed within the magmatic intrusions due to fluid exsolution from the magmas (Burnham，1979)，whereas the fluids in the country rocks may be in hydrostatic regime. The large pressure contrast is likely the main driving force for fluid flow in the early stage (orthomagmatic)of magmatic emplacement，whereas fluid convection due to heat anomaly dominates in the later stage when fluid pressure within the intrusion diminishes toward hydrostatic values (Henley and McNabb，1978). This pressure contrast increases with depth，which may explain why proximal deposits tend to be formed at shallow depths and distal deposits are favored at great depths(Chi et al.，1993). The wide ranges of fluid pressures estimated from fluid inclusions in magmatic-hydrothermal deposits are likely caused by change of fluid pressure from lithostatic or supra-lithostatic within the intrusions to hydrostatic in the country rocks (Chi et al.，1993). Similarly，wide ranges of fluid pressure reported in orogenic gold deposits (Wilkinson and Johnston，1996;Chi et al.，2011)and some base metal deposits in sedimentary basins (Chi et al.，2005，Chi and Xue，2011b)are also interpreted to reflect fluid pressure variation between lithostatic or supra-lithostatic and hydrostatic regimes.However，it is important to make sure that the variation of fluid pressure data from fluid inclusions is not due to post-trapping modification of the fluid inclusions through the use of the fluid inclusion assemblage method (Goldstein and Reynolds，1994;Chi et al.，2005;Chi and Lu，2008).

4 Fluid inclusion plane (FIP)orientation and stress analysis

Hydrothermal mineral deposits are commonly controlled by structures. This is because rock deformation may provide a major driving force of fluid flow，and the increase in rock permeability due to fracturing enhances fluid flow. In numerical modeling of fluid flow related to deformation，it is crucial to know the stress field (Zhang et al.，2006，2011;Cui et al.，2012). Although regional stress field may be inferred from megascopic structural studies，it is uncertain whether the same stress field can be applied during mineralization. The microfractures filled with fluid inclusions，known as “fluid inclusion planes”or FIPs，can provide important information regarding the stress field during mineralization. It has been demonstrated by field and experimental work that FIPs are mostly of extensional origin，or are mode-I microfractures perpendicular to σ3 (Tuttle，1949;Brace and Bombolakis，1963;Tapponnier and Brace，1976;Krantz，1979;Lespinasse and Pecher，1986;Lespinasse，1999). Therefore，by measuring the orientations of a number of FIPs in oriented thin sections and conducting statistical studies，we may infer the stress field during the formation of the FIPs(Lespinasse and Pecher，1986;Boullier and Robert，1992;Lespinasse，1999;Chi and Guha，2011;Liu et al.，2011).Although the inclusions in the FIPs are of secondary origin，it does not necessarily mean that they are late and unrelated to mineralization. In fact，gold mineralization in orogenic gold deposits commonly occurs in microfractures along with secondary inclusions (e.g. ，Robert and Kelly，1987;Chi and Guha，2011;Liu et al.，2011)，suggesting that the secondary inclusions recorded the mineralizing fluids. This concept of secondary inclusions recording mineralizing fluids can be well explained by the fault valve model (Sibson et al.，1988)，and has been illustrated by several examples (Boullier and Robert，1992;Ni et al.，2003;Chi and Guha，2011;Liu et al.，2011). Another advantage of studying FIPs is that fluid pressure may be estimated，as discussed above，in addition to the stress field;it is the combination of stress and fluid pressure that determine whether or not faulting can take place，thus controlling fluid flow，as illustrated in the fault valve model (Sibson et al.，1988).

In many mineral deposits，including notably the orogenictype gold deposits (Sibson et al.，1988;Boullier and Robert，1992)and unconformity-type uranium deposits (Jefferson et al.，2007)，orebodies are hosted by reverse faults or shear zones.Kinetic studies indicate that the faults were formed in a compressional stress regime，with σ1 being horizontal (Fig.4a)or subhorizontal (Fig.4b). However，FIP studies suggest that σ3 was horizontal or subhorizontal，whereas σ1 was vertical or subvertical during certain periods of time in the process of mineralization. For example， in the Sigma gold deposit(Quebec， Canada )， both horizontal-subhorizontal FIPs(dominated by CO2-bearing inclusions)and vertical-subvertical FIPs (dominated by aqueous inclusions)are developed in the veins (Fig.4a)(Boullier and Robert，1992)，the former consistent with a horizontal-subhorizontal σ1，and the latter suggesting vertical-subvertical σ1. Therefore，even though fault valve model can explain the fracturing and fluid movement with the stress regime being maintained horizontal all the time，it is possible that σ1 episodically and locally (mineralization district or deposit scale)switched to vertical during mineralization(Fig.4c). However，it is also possible that the subvertical FIPs resulted from vein- or crystal-scale bridging effect or local detachment of the veins from the wall rocks，as illustrated in

Fig.4 Comparison of regional and local stress fields inferred from megascopic structural and fluid inclusion plane (FIP)analysis(a)megascopic structural analysis indicates horizontal maximum stress (σ1)and vertical minimum stress (σ3)，whereas FIP analysis indicates alternating horizontal and vertical σ1 (based on the study of the Sigma gold deposit by Boullier and Robert，1992);(b)megascopic structural analysis indicates subhorizontal maximum stress (σ1)(perpendicular to foliation)and subvertical minimum stress (σ3)，whereas the dominance of subvertical，foliation-parallel FIPs indicate episodic，subvertical σ1 (based on study of the Red Lake gold deposit by Liu et al.，2011);(c)sketch showing local and episodic vertical σ1 potentially related to increased temperature and reduced density of the fluid reservoir;(d)sketches showing local vertical σ1 due to development of cavities and vein-or crystal-scale bridging effect

Fig.4d (Chi and Guha，2011). In the case of the Red Lake gold deposit (Ontario，Canada)，the FIPs (dominated by carbonic inclusions) are mostly subvertical and parallel to foliation (Fig.4b) (Liu et al.，2011). Although the mechanical anisotropy due to foliation may be invoked to explain the megascopic feature (i.e.，foliation-parallel veins)，as proposed by Kerrich (1989)，it is difficult to explain similar phenomena at microscopic scale，i.e.，FIPs，because no microscopic mechanical anisotropy was observed. Therefore，it may be inferred that the development of the foliation-parallel veins and microfractures resulted from episodic change of local stress field， caused by upward force associated with the overpressured fluid reservoir below the shear zones，perhaps due to increased temperature and decreased density of the reservoir compared to surrounding regions (Fig.4c)(Liu et al.，2011).Similar situation is present in the unconformity-type uranium deposit，where the displacement of the unconformity along the faults hosting the deposits indicate reverse movement (Jefferson et al.，2007)，but basinal fluid flow below the unconformity to form the basement-hosted deposits appear to require an extensional stress regime (Cui et al.，2012). An FIP study may help solve this problem.

5 Fluid temperature constraints on fluid flow models

Because geologic fluid flow is always accompanied by heat transfer，thermal effects recorded by various geothermometers(e.g.， fluid inclusion microthermometry， geochemistry of hydrothermal minerals，and organic matter maturation)can provide important constraints on fluid flow models. The application of fluid temperature on hydrodynamic studies of mineralization may be divided into two types:1)the spatial change of fluid temperature is used to indicate general fluid flow direction，and 2)the thermal patterns (2D or 3D temperature distribution)is used to distinguish different fluid flow models related to different driving forces.

Fig.5 Thermal patterns associated with different fluid flow models related to mineralization(a)deposit-scale thermal profiles，showing three different fluid-rock thermal relationships:1)Tfluid =Trock，2)Tfluid ＞Trock，and 3)Tfluid ＜Trock;(b)regional-scale thermal patterns:1)flat isotherms associated with compaction-driven fluid flow，2)raised isotherms caused by episodic release of overpressured fluids，3)paired raised and depressed isotherms related to topography-driven flow，and 4)undulating isotherms related to heat convection

Fluid inclusion microthermometry，as one of the most popular geothermometers，has been widely used in the studies of various mineral deposits to indicate the fluid flow direction and potentially the sources of the mineralizing fluids. In magmatichydrothermal systems，the trend of decreasing fluid inclusion homogenization temperatures away from the magmatic intrusions is expected，and can be used to infer buried intrusions (Bodnar and Beane，1980). In hydrothermal systems where the source is unknown or controversial，such as the Jinding Zn-Pb deposit hosted in siliciclastic rocks in the Lanping basin (Yunnan，China)， the decrease of fluid inclusion homogenization temperatures away from a regional fault is interpreted to indicate that the mineralizing fluids ascended along the regional fault and then flowed westward to various sites of mineralization (Xue et al.，2007). In classical MVT mineralization provinces in North America，it has been found that the homogenization temperatures of fluid inclusions decrease away from orogenic belts (Leach and Rowan，1986;Qing and Mountjoy，1992). This，together with the Rb-Sr isotopic ages of sphalerite which are comparable to the ages of the orogenies (Nakai et al.，1990;Brannon et al.，1992)，has been taken to indicate that the fluid flow systems responsible for MVT mineralization were driven by the topographic relief associated with the orogenies (Garven and Raffensperger，1997). In other MVT deposits that are not clearly related to orogenic belts，such as in the Maritimes basin in eastern Canada， it appears that the fluid inclusion homogenization temperatures are not systematically varied，suggesting that the fluid flow may have been controlled by individual sub-basins and driven by episodic release of overpressured fluids (Chi et al.，1998;Chi and Savard，1998). Even for the classical MVT districts in the mid-continent of North America， it has been proposed that episodic overpressure-driven (gas pulsars)(Cathles，2007)rather than topography-driven fluid flow is responsible for mineralization.Therefore，although the spatial change of fluid inclusion homogenization temperature，which is of one-dimensional nature，can be used to indicate the overall fluid flow direction，it cannot unambiguously distinguish the driving forces of fluid flow. It is also worth mentioning that for the purpose of determining fluid flow direction，fluid inclusion microthermometry may not be the most efficient method. The decrepitation temperatures of fluid inclusions，which can be obtained rapidly with special thermoacoustic instruments，can also be used to infer fluid flow direction (Baskov，1987).

Different fluid flow systems are characterized by different thermal patterns，and therefore if we can determine the 2D or 3D temperature distribution through fluid inclusion studies or other geothermometers，we may be able to determine the fluid flow mechanism responsible for mineralization among various potential fluid flow models. The thermal patterns may be examined at different scales. At the deposit scale，three kinds of thermal relationships between mineralizing fluids and the host rocks(Tfluid＞Trock，Tfluid=Trock，and Tfluid＜Trock，)may be envisaged(Fig.5a)，as exemplified by the studies of Sangster et al.(1994)for MVT deposits. This can be done through comparison of fluid inclusion homogenization temperatures and thermal indicators in the host rocks such as conodont color alteration index (Sangster et al.，1994)，clay mineralogy and vitrinite reflectance (Héroux et al.，1996;Chi et al.，1998)，and possibly Raman spectroscopy of carbonaceous material (Lahfid et al.，2010). At a regional scale，we can also envisage four kinds of thermal patterns:1)flat isotherms throughout a large region(Fig.5b-1)，typically found in sedimentary basins where fluid flow is dominated by compaction-driven steady flow (Bethke，1985);2)raised isotherms above normal geothermal background over a large area (Fig.5b-2)，which may be caused by rapid and episodic release of overpressured fluid (Cathles and Smith，1983);3)paired depressed (below normal)and raised (above normal)isotherms (Fig.5b-3)，typically found in topographic relief-driven fluid flow systems (Garven et al.，1993);and 4)undulating isotherms (Fig.5b-4)，related to thermal convection(Raffensperger and Garven，1995).

The local thermal patterns may be superimposed on any of the regional patterns. It is impossible to obtain the thermal patterns，either local or regional，and to decipher the mechanism of fluid flow if we limit our studies of fluid inclusions in the mineral deposits. An important part of the debate on fluid flow models related to MVT deposits was concerned with the thermal issues，more specifically on whether or not a fluid flow model can explain the“higher-than-normal”fluid temperatures recorded by fluid inclusions in the MVT deposits (Cathles and Smith，1983;Deming，1992;Garven et al.，1993). However，after three decades of studies，it is still uncertain what fluid flow mechanism was responsible for the MVT mineralization in the mid-continent of North America (Ingebritsen and Appold，2012)，and this is in part due to the lack of information on regional thermal patterns during mineralization. Similar situation is also true for the Proterozoic Athabasca basin (Saskatchewan，Canada)，where world-class uranium deposits have been discovered near the unconformity between the basin and the basement and various fluid flow models related to uranium mineralization have been proposed (Chi et al.，2013)，including compaction-driven flow(Hiatt and Kyser，2007)，topography-driven flow (Derome et al.，2005)，heat convection (Raffensperger and Garven，1995)，and deformation-driven flow (Cui et al.，2012).Again，one of the main reasons for this uncertainty is because most studies have been focused on the mineral deposits，and little information about the regional thermal profile is known (Chi et al.，2013).

6 Duration of mineralization:constraints from fluid inclusions studies

The duration of fluid flow systems associated with mineralization is related to the driving forces. For example，fluid flow systems associated magmatic intrusions (including the orthomagmatic and heat convection stages)are relatively short lived because the intrusions (especially those emplaced at shallow depths)are cooled to ambient temperatures relatively rapidly，thus losing the driving forces，whereas fluid flow systems associated with orogens and topographic relief are likely prolonged because the erosion process is relatively slow.Therefore，knowing the duration of mineralization can also provide constraints on fluid flow models. Unfortunately，the duration of mineralization generally cannot be determined accurately with techniques such as isotopic dating. However，in some cases the combination of fluid inclusion homogenization temperatures with organic matter maturation data may provide an approximate estimation of duration of the fluid flow associated with mineralization，based on the principle that the maturation of organic matter depends on both temperature and time. Using this method，Rowan and Goldhaber (1995)estimated the duration of mineralization in the Upper Mississippi Valley district to be about 200 thousand years.

Another method of estimating the duration of mineralization is based on the principle that the time required to form a deposit of known tonnage of metals depends on the fluid flow rate and the concentrations of metals in the mineralizing fluids (or，more specifically，the change of metal concentrations before and after ore mineral precipitation)(Roedder，1984). Recent fluid inclusion analysis with the LA-ICP-MS method in ore minerals from MVT and Irish-type deposits indicates concentrations of ore elements two orders of magnitudes higher in ore minerals than in gangue minerals (Wilkinson et al.，2009;Appold and Venz，2011)，which suggests much shorter duration of mineralization than previously thought (Bodnar，2009). Similarly，uranium concentrations three orders of magnitude higher than in normal crustal fluids have been found in fluid inclusions from the unconformity-type uranium deposits in the Athabasca basin，suggesting relatively short duration of mineralization (Richard et al.，2010，2012). These new research results provide important constraints on fluid flow models，and represent challenges to existing hydrodynamic theories.

7 Fluid mixing，immiscibility and two-phase flow:More to be learnt from fluid inclusions

Much of our current knowledge about fluid mixing and immiscibility，which are two of the most important mechanisms of ore precipitation， is attributed to fluid inclusion studies(Roedder，1984;Lu et al.，2004;Chi and Lai，2009). The mixing of fluids with different salinities and temperatures is vividly demonstrated by a linear trend in the homogenization temperature-salinity diagram (Roedder，1977;Hayba，1997)，and fluid immiscibility (including boiling)is best evidenced by the coexistence of vapor-dominated and liquid-dominated fluid inclusions (Roedder，1984).

However，most fluid inclusion studies focus on the chemical aspect of fluid mixing and immiscibility，and pay little attention to the physical processes. A detailed study of fluid inclusions in different growth zones with a single sphalerite crystal from Creede(Colorado，USA)by Roedder (1977)suggests that while the overall linear homogenization temperature-salinity correlation may indicate a progressive mixing between a high-T high-salinity fluid and a low-T low-salinity fluid，the composition and temperature change from one growth zone to the next is discontinuous and can be back-and-forth. It is not well known how fast the two fluids must approach each other to cause the physical mixing. Mixing due to basinal fluids flowing through hydrocarbon reservoirs that contain H2S has been proposed as an important mechanism for ore precipitation in many base-metal deposits in sedimentary basins (e.g.，Chi et al.，1995;Xue et al.，2009). However，little is known about the actual mixing process between brine，oil and gas. For example，it is not known how fast the basinal brines must flow to be able to“pierce”into the reservoirs to make the mixing happen.

Similarly，little is known about the physical processes involved in fluid unmixing or immiscibility，which is common in porphyry-epithermal base-metal deposits and orogenic gold deposits. For example，it is not well known whether the two immiscible phases will follow two different pathways after unmixing，or they will flow together as a two-phase flow. This is important for understanding the relationship between porphyrytype and epithermal mineralization (Heinrich，2005)，and the relationship between orogenic gold deposits emplaced at different crustal depths (Groves et al.，1998). The significance of the observation that CO2-rich and aqueous fluid inclusions are separated in microfractures of different orientations (Boullier and Robert，1992)has not been fully understood. More fluid inclusion studies purposely designed to tackle these questions are needed. For example，comparison of fluid inclusion data(Kostova et al.，2004)with results of numerical modeling of multiphase fluid flow (Hayba and Ingebritsen，1997)may provide insights into the physical processes of multiphase fluid flow (Driesner and Geiger，2007).

8 Conclusions

Fluid inclusion and hydrodynamic studies of mineralization share the same interest in fluid pressure，temperature，density and composition， or PVTX. This fundamental relationship underlines the applicability of fluid inclusion studies to fluid flow models. Fluid inclusion studies have contributed to the development of hydrodynamic models of many mineralization systems，especially in estimating fluid pressure regime and in linking spatial change of temperature with potential fluid flow driving forces. However，most of these contributions were made in a passive way，i.e.，fluid inclusion studies were conducted initially for purposes other than hydrodynamic studies. In the future，more fluid inclusion studies may be purposely designed to answer questions related to fluid flow models， such as determination of the fluid flow driving forces，the physical process of mixing，phase separation and multiphase flow.

Acknowledgements This paper has been presented at the 34thInternational Geological Congress (August 5-10， 2012，Brisbane)and the 17thNational Conference on Fluid Inclusions and Geofluids Research in China (November 13-14，2012，Hangzhou);I would like to thank all the colleagues who provided feedbacks during the conferences and Dr. Pei Ni for the invitation. My research on fluid inclusions and hydrodynamics of geofluids is mainly supported by NSERC-Discovery.

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