Mapping of Venus

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Global surface of Venus

The mapping of Venus refers to the process and results of human description of the geological features of the planet Venus. It involves surface radar images of Venus, construction of geological maps, and the identification of stratigraphic units, volumes of rock with a similar age.

Satellite radar provides imagery of the surface morphology by using the physical properties of wave reflection. Long wavelength microwaves are used to penetrate the thick, cloudy atmosphere of Venus and reach to the surface. Different surface features reflect waves with different strengths of signal, producing images from which the maps are constructed.

After collection of the images of the Venusian surface, scientists started to map and identify different geologic materials and units according to distinctive surface features. Different groups of scientists analysed different mapping areas, schemes and interpretation of features observed, to produce a classification of the units and comparison of their mapping.

Background

Before Magellan

Venusian cloud structure captured by the Pioneer Venus Orbiter using ultraviolet in 1979.

Main Article: Observations and explorations of Venus, Venera

Before the development of radar ground-based observation, the thick yellow atmosphere hid detailed Venusian surface features.[1] In the 1920s, the first Venus ultraviolet project captured the thick atmosphere of Venus, but provided no information about the surface.

From 1961 to 1984, the Soviet Union developed the Venera probes for surface mapping by radar. The Venera 4 (on October 18, 1967) was the first man made lander to make a soft landing through the atmosphere on Venus (also the first for other planetary objects). The probe only survived for at most 23 minutes before being destroyed by the Venusian atmosphere. The Venera series space probes returned images of the Venusian surfaces,[2] shown as below with the landing locations of the probes.

Position of Venera landing sites and the radar topography obtained. Red points denote sites returning images from the surface, black central dots sites of surface sample analysis.

Magellan Mission

Synthetic Aperture Radar (showing right-looking in this diagram).

Main Article: Magellan (spacecraft), Synthetic aperture radar

The surface of Venus was mapped in detail by the Magellan Spacecraft in 1990-91. The spacecraft orbited around Venus and captured images of the adjacent surface. During three orbits, the surface image were transmitted back to the Earth. These three orbiting motions of the spacecraft are called cycle 1, 2 and 3.

During the cycle 1 (left-looking) radar surface mapping on Venus (September 15, 1990 to May 15, 1991), around 70% of the Venusian surface was mapped by Synthetic aperture radar. In cycle 2 (right-looking), 54.5% of the surface was mapped, mainly the south pole regions and gaps from cycle 1 during May 15, 1991 to January 14, 1992. Combining cycle 1 and 2 results in a total coverage of 96% of Venusian surface mapped. Cycle 3 (left looking) filled remaining gaps and collected stereo imagery of approximately 21.3% of the surface, increasing the total coverage to 98%.[3][4][5]

SAR image on Venus. This map is a mosaic of the "left-looking" data collected during cycle 1, produced by the USGS of the Magellan images.

Proposed Future InSAR Mapping

Main Article: Interferometric synthetic aperture radar

NASA InSAR satellite measuring small scale earthquakes

The use of Interferometric synthetic aperture radar (InSAR) for mapping Venus has been proposed.[6]

Instead of surface mapping by SAR discussed above, InSAR is used to measure the terrain motions during events (such as earthquakes or tectonic movements). By performing the radar mapping at two separated times (before and after an event) over the same area, the terrain shift will be shown as different phase due to path difference in the radar echo returned.[6][7]

However, there are recently no new planetary missions to Venus announced. It maybe a possible future work can be done to explore more about this planet and its potential tectonic movements.

Construction of Map

Main Article: Radar mapping Synthetic aperture radar

From the Magellan mission data, 3 types of images have been produced: (1) SAR images, (2) topographic images and (3) meter scale slope image.[7][8]

SAR Images

SAR images is the most important base map for mapping as the highest resolution data set. Microwave are used to penetrate the thick atmosphere and map the surface of Venus.

The SAR images are white and black images, which shows the surface features using the intensity of radar return (echo), either due to surface roughness or orientation.[7]

If the surface is rougher, the radar will be scattered away and the intensity of echo will be weaker, which are represented by brighter regions in normal SAR images. On the other hand, if the surface is smoother, the wave will be reflected along the same direction, resulted as a higher intensity of echo and represented by darker regions.

Difference in wave reflection on smooth and rough surfaces.

The orientation of surface is depends on the looking direction of the radar. Unlike satellite images of Earth surface, SAR images tells no clues on the color of surface, but the reflection of wave on the surface at a particular looking direction (direction of wave propagation). For example, when there is a light source shining on the blue cap on the left (left-looking), there will be shadows on the another side of the cap where light wave are blocked by the cap and no reflection occurs. If the looking direction is changed to the right, the shadowing (dark on SAR image) part will be at the opposite side.

Real life example on difference in looking direction in SAR images. Same object with difference looking direction shows completely different result in SAR image.
Left (left-looking) and right (right-looking) images showing the difference in SAR images on the same location on Venus. (Venus images extracted from USGS)

The USGS Branch of Astrogeology[9] has produced a full resolution radar maps (also known as FMAPs) of Venus from the SAR data collected from the Mission, called the Magellan F-BIDRs (Full resolution Basic Image Data Records). The maps has a coverage of around 92% (combination of the 2 left-looking cycles).[3][10] The resolution of it is 75 m/pixel, which is the highest resolution of Venusian map.

Topographic Maps

Topographic images were collected using radar altimetry. Compared to the SAR images, the topographic image has a significantly lower resolution of around 3–5 km/pixel. These images show lower elevations with darker pixels with higher elevation is shown by brighter pixels. Despite of the low resolution, it is useful to study the regional feature of Venus, including initial evidence for the existence of rift zones.[7]

Topographic Map of Venus

Topography

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Main article: Geology of Venus

There are three types of topography on Venus

  1. Highlands with elevation greater than 2 km, cover about 10% of the surface
  2. Deposition Plains with elevations around 0 to 2 km, cover more than 50% of the surface
  3. Lowlands (accumulation of eroded highlands) with negative elevation, cover the rest of the surface

The surface observation include impact craters, volcanoes and lava flow channels, which give clues to estimate the surface age, possible global resurfacing events, tectonic activities, internal structure and surface processes.

Unit classification and mapping schemes

There are many groups of workers who have mapped the surface of Venus after the Magellan Mission. Different groups mapped different cartographic quadrangles of the surface of Venus. They applied different mapping schemes and came up with different classifications of Venusian units.

Here is a table comparing the different mapping scheme and unit identification of the Magellan Science Team (1994),[11] Vicki L. Hansen (2005)[12] and Mikhail A. Ivano and James W. Head (2011).[13] The possible matching of the above units are in accordance with their radar back scatter and surface features.

Mapping Groups Magellan Science Team (1994) Mikhail A. Ivanov and James W. Head (2011) Vicki L. Hansen (2005)
Mapping Scheme Global-scale geologic mapping scheme

(defined by difference in radar back scatter, surface texture and topographic)

 Stratigraphic Classification Scheme

(defined to global stratigraphy with a division of geologic time)

 (defined by local formations and deformations, instead of global stratigraphic)
Unit Classification Stratigraphic Units: Stratigraphic Unit
(Tessera is not in this classification) 1. Tessera (t) 1. Tessera terrain

(Further classification into 7 types, according to the features in Hansen and Willis' paper in 1996[14])
2. Mountain belts (mb)
1. Lineated plains 3. Densely lineated plains (pdl) 2. Flow material from different origin locally
2. Reticulate plains 4. Ridged plains (pr)
/ 5. Regional plains (rp, upper and lower units)
3. Bright plains /
4. Dark plains 6. Smooth plains (ps)
5. Mottled plains 7. Shield plains (psh)
8. Shield clusters (sc)
6. Digitate plains (lava flow fields) 9. Lobate plains (pl)
Geomorphic Units: Structural features
1. Complex ridged terrain (CRT or tesserae) (Tesserae is a geological material instead of structural features)
2. Ridged and fractured terrain
3. Ridge belts (including mountain belts) 1. Groove belt (gb) 1. Secondary Structures
4. Fracture belts
/ 2. Rift zones (rz)
Deposits:

- Associated with impact events

 Impact Crater Forming Materials
1. Crater material 1. Crater materials (c) 1. Crater material
2. Bright diffuse deposits 2. Impact crater flow material (cf) 2. Flooded crater material
3. Dark diffuse areas

The details of the above mapping scheme and units will be discussed one by one below.

Geologic mapping scheme by the Magellan Science Team

The global-scale geologic mapping scheme by the Magellan Science Team was a very early mapping done after the Magellan Mission (1990-1991). Instead of identifying different geological materials, it basically grouped the global surface units with different radar back-scatter (white and dark in SAR images), topography and surface texture.

The mapped units and their characteristics are listed below.

Stratigraphic units

The stratigraphic units in this mapping scheme are classified as 6 types of plains:

Stratigraphic Units
Units Radar Back-scatter Surface features Interpreted Geological materials
Lineated plains Moderate and homogeneous Abundant fractures, forming grids or orthogonal patterns /
Reticulate plains Intermediate and homogeneous Abundant and low sinuous ridges /
Dark plains Homogeneous, dark local areas Smooth Lava flow
Bright plains Homogeneous, bright local areas / Lava flooding with extension and rifting
Mottled plains Extensive areas with both bright and dark materials Mottled textures with abundant small shields and despoites /
Digitate plains Bright and dark deposites In digitate patterns Lava flow fields associated with coronae

Geomorphic Units

The units are defined by groups of structural features of commonly higher elevation area with ridges and deformations:

Geomorphic Units
Units Complex ridged terrain (CRT or tesserae) Ridged and fractured terrain Ridge belts Fracture belts
Surface features Ridges and fractures with deformations Same as CRT, but with a single direction of deformations dominate Linear, which parallel to the nearby ridges Dense parallel linear fractures, mainly around equatorial and southern regions
Topography Regional highland areas Regional highland areas Elevated rudges /
Images
Aphrodite Terra Complexly deformed
Lineated terrain Alpha Regio
Northern part of the Akna Montes (mountains) of Venus with a ridge belt.
Lineated Plains on Venus

Deposits

The deposits are mainly the impact crater materials and its deposits:

Deposits
Units Radar Back-scatter Surface Features Image
Crater material Radar-bright impact crate ejected materials /
Mapping of Venus Crater based on 3 units: (1) crater material (2) bright diffuse deposits and (3) dark diffuse deposits.
Bright diffuse deposits Radar-bright materials Forming "wispy patterns"
Dark diffuse deposits Radar-dark materials Parabola in shape

Stratigraphic classification scheme

One way to do mapping on Venus and characterization on the geological units on Venus is by the stratigraphic classification scheme.[15] Mikhail A. Ivano and James W. Head (2011) mapped the area of geotraverses at 30N[16] and 0N. They traced and discussed the global spatial distribution of rock-stratigraphic units and structure, and suggested their time correlation and geological history.[13]

Stratigraphic units

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Main article: Stratigraphic unit

This mapping scheme suggested that there are around 12 global units on Venus by the work of Mikhail A. Ivano and James W. Head (2011), and these units are used throughout their mapping on different quadrangles on Venus. The stratigraphic units and landforms mapped by Mikhail A. Ivano and James W. Head (2011)[13] are listed below in terms of mechanism from the oldest to the youngest.

Tectonic units

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Main article: Tectonics

Tectonic units are formations formed due to large-scale crustal processes. In this mapping scheme, these surface units are grouped into possible same set of geological materials, shown by similar surface features.

Tessera (t)

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Main article: Tessera (Venus)
Outline of tessera terrain imposed on "GIS Map of Venus" (GIS Map of Venus source: USGS Astrogeology Science Center)
Maxwell Montes's tessera (t) terrain seen in appearing as white in SAR image

Tesserae are heavily deformed highland regions (greater than 2 km in elevation) on Venus. This unit is believed to be the oldest material on Venusian surface with highest level of tectonic deformation.[17][18] It is of high topography and seen in white on the SAR images with high radar backscatter.[19] The materials composed tessa terrain, which was named as unit Tt in the mapping of V-17(Basilevsky, A. T.,1996).[20]

The intersecting of material and tectonic structures are the defined characteristic of tessera, but the sets are not always seen in the images.[13] Due to the heavy tectonic deformation, it contains both contractional features of ridges and extensional features of graben and fractures.[13]

The boundaries of tessera shows embayment by other materials of other units. By this cross-cutting relationship, it provides evidence of tessera being the oldest unit within the strata.[13]

Densely lineated plains
Densely lineated plains (pdl) on Venus

The densely lineated plains unit (pdl) is defined by the dense and parallel lineaments packed on the unit.[13] They make up a small area on Venus's global surface of around 7.2 x 108 km2.[13] The lineament is the pattern of deformation, which make it a typical structural–material unit.[13]

There is evidence showing the embayment of tessera by pdl's material in some tessera margins. Thus, it is possible that this unit is younger than the tessera unit.[13]

In SAR images, it also shows a high backscatter imagery, but lighter than that of tessera.

Ridged plains (pr)
The ridge belt that forms in the western part of the elevated smooth plateau of Lakshmi plain.

The ridged plains unit are lava plains deformed by ridges. They have a smooth surface with relatively higher elevation than the surroundings.[13] The ridges are usually symmetrical in cross-section and collected into prominent belts.[21][22]

There is evidence in places showing that pr unit is embaying the t and pdl unit. Also, the deformation of pr took place after the formation of t and pdl units. Thus, pr unit is possibly younger than both unit t and pdl.[13] As most of the deformation features on pr is far away from that on t and pdl units, it is difficult to tell the age relationship of deformation directly.[23][24][25] However, there are some tessera-like deformations additional to the ridge belts, it suggests there are some possible overlapping of formation time in unit t and pr.[13]

In SAR images, pr units have noticeably higher radar backscatter than surrounding regional plains, but lower than tessera (t) and densely lineated plains (pdl) units. Ridges planes have older ages compared to surrounding regional plains (pr) due to the difference in radar albedo and embayment relationships suggested by McGill and Campbell (2006).[26]

The major occurrence of this unit is located among Vinmara, Atalanta, Ganiki, and Vellamo Planitiae, shich in a broad fan-shape,[27][28][29][30] and also appears between Ovda and Thetis Regiones and in the southern hemisphere within Lavinia Planitis.[31][32]

Some researchers mapped ridges of the pr unit as deformed structures instead of a unit.[33][34][35][36][37]

Mountain belts (mb)
Perspective View of Ishtar Terra showing the mountain belt (mb) units with Akna Montes and Freyja Montes along the western and northwestern edge of Lakshmi Planum, and Maxwell Montes along its eastern edge.

The mountain belts unit is the only real mountain range on Venus in the area surrounding Lakshmi Planum, which covers only 1.3 x 106 km2 of the Venusian global surface,[27][38][39][40][41] while involves structural deformation of different materials in their formation.[13] There are in total four major mountain belts mapped on Venus, including the belts of Danu Montes, Akna Montes, Freyje Montes and Maxwell Montes (the highest mountain on Venus with elevation of around 12 km).[13]

When looking at the cross-cutting relationship, the inner ridges of the belts seems to be embayed by the material of regional plains (pr), which covered the plateau surface. There is later deformation in terms of tilting towards the belts and wrinkle ridges parallel to the belt. It suggested formation formed right before the deposition of regional plains and later deformation of the belts.[13]

Shield plains
Formation of Shield Domes.
Accruva Formation. Evaluation Diagram of Shield plain formation from Shield Domes over time.

The shield plains units (psh) refers to plains with volcanic edifices of shield-like features.[42][43][44] In most of the psh regions. the plains are concentrated and forms a group. It is the oldest unit in the strata showing no widespread deformation, in which only little tectonic deformation is observed, such as ridges and fractures.[13] Compared to the above units, this unit seems to cover a high proportion of the Venusian surface at around 79.3 x 106 km2. Although the distribution of psh is widely spread and homogeneous, there are also some regions with no psh units, including the Lakshmi Planum and some lowland of regional plains,[13] The shield plains are formed from shield domes over time and suggested that psh may be associated as volcanic plains with small sources of volcanic materials and mildly deformed by tectonics.[13]

There are embayment relationships, showing that this unit is younger than the above highly tectonized units (t and pdl) at a global scale. However, the absence of the unit in some regions makes this unit difficult to fit into the strata, especially between the highly tectonized units mentioned above, and regional plains which will be mentioned in the next section.[13]

In SAR images, the psh unit shows a higher radar backscatter compared to surrounding overlaying regional plains, still lower than units of t, pdl and pr.[13]

Regional Plains (rp)

The Regional Plains unit (rp) is the most wide spread unit on the Venusian surface of about 182.8 x 106 km2.[13] It is defined as smooth and homogeneous plains, which are deformed into networks of linear subparallel or intersecting ridges.[45] This unit is interpreted as having volcanic origin with deformation of wrinkle ridges superimposed. However, the source of volcanism is not obvious in the Magellan data.[13]

Regional Plains are divided into abundant lower unit (rp1, Rusalka Formation) with smooth surface and relatively low radar backscatter and upper unit (rp2, Ituana Formation) with also smooth surface, but higher radar albedo. Wrinkle ridges heavily deform the lower unit while moderately deforming the upper unit. The lower unit is heavily tectonized and embayed by lava plains and flows. The younger upper unit is lacking in large heavily tectonized tessera regions.[13]

In SAR image, it shows an intermediate level of radar backscatter.

Shield clusters
Volcanic Domes on Venus

The Shield clusters unit (sc) is similar to shield plains, but tectonically undeformed. Based on the analysis by Crumpler and Aubele (2000),[46] 10% of this unit shows evidence that it is younger than regional plains (rp).[47] Some of the small shield clusters are founded embaying the regional plains of both lower and upper layers, while in some regions, this unit is found on top of the rp unit and deformed together by wrinked ridges.[13]

Smooth plains
Adivar crater. Dark (Smooth plain) deposition around the crater.

Th Smooth plains unit (ps) belongs to Gunda Formation, which is a smooth and featureless surface without tectonic marks. It only makes up about 10.3 x 106 km2 of Venusian surface. These plains are usually do not have impact craters, which is tectonic undeformed.[13] These plains are rarely with low domes. These suggested three type of setting for this unit:

(1) Many fields of smooth plains are near to the regions with young volcanism (such as Bell Regio) with the lobate plains (pl). However the relationship of smooth and lobate plains is uncertain.

(2) Some of the unit is located as deposition around an impact crater, possibly associated with the impact events.[48][49]

(3) small ps units are inside the tessera regions (such as Ovda Regio), which may associate with a volcanic origin,

Due to the usual higher elevation of smooth plains, it is possible that the volcanic material of smooth plains is a younger unit.[13]

Lobate plains

The Lobate plains unit (pl) is a smooth surface crossed with some extension features associated with rift zones. These features make up to around 37.8 x 106 km2, which is significant. The origin of lobate plains is believed to be associated with large volcanoes, which sometimes appear with large dome-shaped rises.[13] One possible origin of this unit is from massive and multiple eruptions from large and localized volcanoes with little later extensional deformation.[13]

By cross-cutting relationships, the plains embay the wrinkle ridges containing regional plains, which suggested that lobate plains are younger.[13] However, as the lobate plains, smooth plains, shield cluster and rift zones are often seen as small fractures, it is difficult to tell their time relationship.

In SAR image, they shows uneven radar back-scatter flow-like pattern.

Structural Units

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Main article: Structural geology

Structural units are formed due to deformation. The resultant properties depend on the stress applied to the formation and the stain of the rocks.

Tessera-forming structures (ridges and grooves)

Ridge structures are mainly discussed in the ridged plains (pr) part above.

Groove belts (gb) belong to the Agrona Formation, which refers to dense extensional structures. This unit appears to be sets of subparallel lineaments of fractures or grabens.[13] This deformation unit makes up to around 37.1 x 106 km2 of the Venusian surface. These fractures are the most obvious and are very abundant on the surface of Venus, and crosses different units on the surface. It appears to be a younger unit on the surface. However, some vast plains units are found embaying the grooves in some areas. It suggests the formation of gb unit before the formation of plains.[13]

The major difference between grooves unit and dense lineated plains are that the former is belt-like and the latter is patch-like.[13]

It is very important to map these fractures, as sometimes the rock unit may be too deformed and is not recognizable, which it can be mapped as "fractured plains materials" according to the guidelines of Wilhelms (1990).[50]

In SAR image, these fractures are of high radar albedo, as high as that of the tessera unit.[13]

Rift zones

The Rift zones unit (rz) belongs to the Devana Formation, which is also made up of dense extensional structures with defined numbers of fissures and troughs containing flat-floors.[13]

It is found that the rift zones are usually related to the lobate plains, which may indicate that the rifting is related to the young volcanism and also young volcanic plains formed.[13]

Impact Crater Forming Materials
Dickinson Crater on Venus. The structure can be clearly seen.

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Main article: Impact crater

Just like the impact crater on Earth and other terrestrial planetary bodies, impact craters on Venus include central peaks, rims, floors, walls, ejected deposits and outflows from the craters. There are two groups of materials, including undivided crater materials (c) and impact crater flow material (cf).[51]

The study of impact craters on Venus is important to discover its geological history. In testing the model of catastrophic and equilibrium Model (another hypotheses instead of global stratigraphy[52]) on Venus, it is found that the older regional plains (rp) are embaying only around 3% of the impact craters and the younger lobate plains (pl) are embaying around 33% of the impact crater on Venus. It suggested that there are likely to have been at least two geological periods on Venus:

(1) Earlier global volcanic regime stage (Formation of older regional plains), when the high rate of volcanic activities overwrote the marks of impact cratering

(2) Later network-rifting and volcanic regime stage (Formation of younger lobate plains), when the intensity of volcanism is reduced and allowed more impact cratering to beleft on the surface.

Thus, the studying of crater distribution and randomness may give clues for Venusian geological history.[53]

Global stratigraphy

A simple Venus global strata base on Ivanov and Head's model (2011). (Note that it is just a simple global strata, not every region on Venus has this strata.)

Under the Global stratigraphic Classification Scheme, by correlating the units mentioned above (Mikhail A. Ivano and James W. Head, 2011),[13] the researchers suggested three phases of Venusian geological history:

(1) The earliest period, Fortunian Period, involved intensive formation of tessera (t) (building of thick crust at the same time).

(2) Then, it came to Guinevere Period, which firstly, there was formation of Atropos (dense lineated plains, pdl), Lavinia (Ridged plains, pr), Akna (Mountain belts, mb), and Agrona (groove belt, gb). Later, there was global emplacement of Accruva (shied plains, psh), Rusalka (lower regional plains, rp1), and Ituana (upper regional plains, rp2) Formations. There are events of wrinkle ridges formed around the global. Mostly of the surface of Venus was resurfaced in this period

(3) In the Altlian period, there are limited formations of smooth plains (ps), Gunda Formation, and shield clusters (sc), Boala Formation, possibly due to Atlian volcanism. There was significant reduction in the rate of volcanism and tectonism.[13] However, these proposed events, and formation of units are not yet fully explained by a complete Venus geological model, such as resurfacing of Venus or heat-pipe hypothesis.

The mapping scheme by Vicki L. Hansen (2005)

The mapping scheme applied by Vicki L. Hansen is mainly regional based, instead of using global stratigraphy as Mikhail A. Ivano and James W. Head did. This mapping scheme focuses on the regional origin of geological materials.[14]

Tectonic units

There are only two major units classified under this group. These two units are further classified below:[14]

Tessera Terrain

Tessera terrain is seen locally the oldest unit on Venus.

It can be further classified into eight groups according to the deformation features:[14]

  1. Fold Terrain
  2. "Lava Flow" Terrain
  3. S-C Terrain
  4. Extended Fold Terrain
  5. Folded Ribbon Terrain
  6. Basin-and-Dome Terrain
  7. “Star” Terrain
  8. Tessera Inliers

Some of the terrains have multiple deformations, but it is not essential for them to have complex deformation.[14]

Flow materials with different origins

The relatively low-lying plains are mapped as flows from different origins locally. These material are believed to be thick young sediments deposited rapidly. In SAR images, the flows material can be both radar-dark or bright.[14]

Structural features

Structural deformation is treated as a feature instead of a unit.[14]

There are some common features mapped, such as linear fractures, ridge and wrinkled ridge identified in many regions, and other local features only found in some regions, such as dome, belt fractures, ribbon, graben, etc.[14]

Impact Crater Forming Materials

The classification of impact crater forming materials are (1) crater materials and (2) flooded crater materials,[12] which is similar to the Stratigraphic Classification Scheme.

Controversial difference between different mapping scheme

Here are difference on terminology and classification of units:

(1) The term "Complex ridged terrain (CRT or tesserae)"

(2) Treating tessera terrain as a global stratigraphic unit

(3) Terminology and classification of "plains"

The terminology of "Complex ridged terrain (CRT or tesserae)"

Hansen (2005) suggested that the tessera terrain should not be named as "complex ridged terrain (CRT)". For the term "complex ridged terrain (CRT)" used by the Magellan Science Team (1994),[11] it carries confusions.[12] Ridges can be also understood as fold. Fold is a contractional features. However, not all tessera deformation are due to contraction.

Treating tessera terrain as a global stratigraphic unit

For treating tessera terrain as the oldest global unit in the Stratigraphic Classification Scheme, it is questioned under Hansen (2005)'s mapping scheme.[12] Although it is commonly the oldest unit mapped in different Venusian areas, it may not be the case for everywhere. The assumption of all the tessera are formed at the same time and the oldest around the global are remained untested.

Terminology and classification of "plains"

There are a major difference in terminology between the Stratigraphic Classification Scheme and Hansen (2005)'s mapping scheme, which Hansen (2005) suggested that "fold material" should be used instead of "plains with different surface features". It can be explained by three reasons:[12]

  1. "Plains" is not used to describe geological material, but surface physical features.
  2. Also, according to fundamental geological mapping principles, secondary structure (such as lineated,ridged and wrinkled) should not be used to define geological units.
  3. There is no evidence that the Venusian plains are volcanic products resulted from extensive flood lava

Thus, in Hansen's mapping scheme (2005), plains are defined as flow from different local origins in regional mapping.

Quadrangles' Mapping of Venusian Geological Units (Regional Mapping)

Quadrangles on Venus

The quadrangles mapping and classification of geological units by different groups of researchers are mainly based on regional units mapped locally. Different groups have their own grouping of units, which are not fully coherent with others work and the proposed global stratigraphy. Also, there are some regional features being classified regionally.

Cartography

The United States Geological Survey defines sixty two cartographic quadrangles for the surface of Venus,[54] with V-1 as the north pole region and V-62 as the south pole region. Base on the FMAPs, different groups of Venus researchers are mapping different quadrangles for the surface of Venus, resulting in different type of units defined.

Here are some examples of quadrangle mapping and their ways of classifying and grouping observed geological units. Some of them are having a similar time sequence as the global stratigraphy mentioned above and will be highlighted below.

Examples of Quadrangle Mapping Unit classification

Here are the list of examples comparing the mapping schemes and units in quadrangles (regional mapping):

Quadrangles Mapping Groups, Year of Publishing Mapping Scheme Stratigraphic Units Identified Structural Units Mapped Other Information
V-5 Barrymore Quadrangle Mapping[55] Elizabeth Rosenberg and George E. McGill, 2001 Similar to the global stratigraphic mapping scheme with the oldest tessera, followed by dense lineated materials, up to other younger plains materials.
  • Plains materials (p, local plains and regional plains of different features)
  • Flow materials (f)
  • Corona materials (co)
  • Linear belts (bl)
  • Dense lineated materials (ld)
  • Terrera materials (t)
  • Impact crater materials (c)
  • Linear belts
  • Wrinkle ridges
  • Radar-bright
  • Linear features
  • Coronae
  • Corona-like features
 /
V-13 Nemesis Tesserae Quadrangle Mapping[51] Mikhail A. Ivanov and James E. Head, 2005 Global Stratigraphy Units Classification
  • Plains materials of dense lineated plains (pdl), ridged and grooved plains (prg), shield plains (psh), wrinkle ridged plains (pwr) and smooth plains (ps)
  • Tessera material of tessera unit (t)
  • Crater material of undivided crater materials (c) and impact crater flow material (cf)
 / /
V-35 Ovda Regio Quadrangle Mapping[56]
Ovda Regio in V-35.
 Leslie F. Bleamaster, III, and Vicki L. Hansen, 2005 Mapping by grouping local formations and deformations, instead of global stratigraphic
  • Western regions (mainly flow materials with different origin and Ovda Regio tessera terrain )
  • Northeastern region (mainly flow materials with different origin and tessera terrainof Thetis Regio and undivided part)
  • South-central to southeastern region (mainly flow materials with different origin and Boszorkany Dorsa basal material)
  • Widespread units (Chasmata flow material, crater material, flooded crater material and tessera inlier terrain)
 /
  • Regionally, the tessera unit are also the oldest unit with younger flows embaying it.
V-48 Artemis Chasma Quadrangle Mapping[57] Roger A.Bannister and Vicki L.Hansen, 2010 Mapping by grouping local formations and deformations, instead of global stratigraphic
  • Crater materials (c)
  • Flow and shield materials (f)
  • Tectonic and fracture terrain units (fr, t)
  • Radar unit (rf)
 /
  • Tectonic and fracture terrain units is the oldest unit as it is mainly the tessera unit.
  • All crater material and radar unit forms throughout the whole time period.
  • The radar units are the high backscatter radar facies marked by penetratively developed, and it does not represent single geological units,

Examples of Regional Geological Mapping

Here is an example of geological map in quadrangle V-20. The units are classified as (1) tessera material, (2) plains materials, (3) materials of coronae and (4) materials of domes and miscalleneous flows, with structures like ridges, wrinkle ridge and lineations.

Ｇeological Map of V-20 Original SAR Image of V-20
V-20 Venus Geologic Map.
Irnini Mons on Venus (V-20)

References

  1. ↑ Ross, F. E. (1928). "Photographs of Venus". Astrophysical Journal. 68–92: 57
  2. ↑ Goldstein, R. M.; Carpenter, R. L. (1963). "Rotation of Venus: Period Estimated from Radar Measurements". Science. 139 (3558): 910–911.
  3. ↑ 3.0 3.1 Howington-Kraus, E., Kirk, R. L., Galuszka, D., & Redding, B. (2006). “USGS Magellan stereomapping of Venus”. In European Planetary Science Congress 2006 (p. 490).
  4. ↑ "Mission Information: MAGELLAN". NASA / Planetary Data System. 1994-10-12. Retrieved 2011-02-20.
  5. ↑ Grayzeck, Ed (1997-01-08). "Magellan: Mission Plan". NASA / JPL. Retrieved 2011-02-27.
  6. ↑ 6.0 6.1 Meyer, Franz J., and David T. Sandwell. "SAR interferometry at Venus for topography and change detection." Planetary and Space Science 73.1 (2012): 130-144.
  7. ↑ 7.0 7.1 7.2 7.3 Kazuo, O. "Recent Trend and Advance of Synthetic Aperture Radar with Selected Topics: Remote Sensing." (2013): 716-807.
  8. ↑ Graff, Jamie R. MAPPING AND ANALYSIS OF THE TECTONO-MAGMATIC FEATURES ALONG THE HECATE CHASMA RIFT SYSTEM, VENUS. Diss. Carleton University Ottawa, 2014.
  9. ↑ Herrick, R. R., & Sharpton, V. L. (2000). Implications from stereo‐derived topography of Venusian impact craters. Journal of Geophysical Research: Planets, 105(E8), 20245-20262.
  10. ↑ Howington-Kraus, E., et al. "USGS Magellan stereomapping of Venus." European Planetary Science Congress 2006. 2006.
  11. ↑ 11.0 11.1 Senske, D. A., Saunders, R. S., & Stofan, E. R. (1994, March). The global geology of Venus: Classification of landforms and geologic history. In Lunar and Planetary Science Conference (Vol. 25, p. 1245).
  12. ↑ 12.0 12.1 12.2 12.3 12.4 Hansen, V. L. (2005). Venus's shield terrain. Geological Society of America Bulletin, 117(5-6), 808-822.
  13. ↑ 13.00 13.01 13.02 13.03 13.04 13.05 13.06 13.07 13.08 13.09 13.10 13.11 13.12 13.13 13.14 13.15 13.16 13.17 13.18 13.19 13.20 13.21 13.22 13.23 13.24 13.25 13.26 13.27 13.28 13.29 13.30 13.31 13.32 13.33 13.34 13.35 13.36 13.37 Ivanov, Mikhail A., and James W. Head. "Global geological map of Venus." Planetary and Space Science 59.13 (2011): 1559-1600.
  14. ↑ 14.0 14.1 14.2 14.3 14.4 14.5 14.6 14.7 Hansen, V. L., & Willis, J. A. (1996). Structural analysis of a sampling of tesserae: Implications for Venus geodynamics. Icarus, 123(2), 296-312.
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  16. ↑ Ivanov, Mikhail A., and James W. Head. "Geology of Venus: Mapping of a global geotraverse at 30 N latitude." Journal of Geophysical Research: Planets 106.E8 (2001): 17515-17566.
  17. ↑ Ivers, Carol; McGill, George. "Kinematics of a Tessera Block in the Vellamo Planitia Quadrangle". Lunar and Planetary Science. 29
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  19. ↑ Bindschadler, Duane; Head, James (1991). "Tessera Terrain, Venus: Characterization and Models for Origin and Evolution". Journal of Geophysical Research. 96 (B4): 5889–5907.
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  23. ↑ Gilmore, M.S., Head, J.W., 2000. Sequential deformation of plains at the margins of Alpha Regio, Venus: implications for tessera formation. Meteoritics Planet. Sci. 35, 667–687.
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  25. ↑ Basilevsky, A.T., 2008. Geologic map of the Beta Regio quadrangle (V-17), Venus. U.S. Geological Survey Sci. Inv. Map 3023
  26. ↑ McGill, G.E., Campbell, B.A., 2006. Radar properties as clues to relative ages of ridge belts and plains on Venus. J. Geophys. Res. 111, E12006. doi:10.1029/ 2006JE002705.
  27. ↑ 27.0 27.1 Barsukov, V.L., Basilevsky, A.T., Burba, G.A., et al. (24 others), 1986. The geology and geomorphology of the Venus surface as revealed by the radar images obtained by Venera 15 and 16. J. Geophys. Res. 91, D399–D411.
  28. ↑ Frank, S.L., Head, J.W., 1990. Ridge belts on Venus: morphology and origin. Earth Moon Planets 50/51, 421–470.
  29. ↑ Kryuchkov, V.P., 1990. Ridge belts: are they compressional or extensional structures? Earth Moon Planets 50/51, 471–491.
  30. ↑ Kryuchkov, V.P., 1992. Ridge belts on plains. In: Barsukov, V.L., Basilevsky, A.T., Volkov, V.P., Zharkov, V.N. (Eds.), Venus Geology, Geochemistry, and Geophysics (Research Results from the USSR). University Arizona Press, Tucson, London, pp. 96–112.
  31. ↑ Squyres, S.W., Jankowski, D.G., Simons, M., Solomon, S.C., Hager, B.H., McGill, G.E., 1992. Plains tectonism on Venus: the deformation belts of Lavinia Planitia. J. Geophys. Res. 97, 13579–13599
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  33. ↑ Johnson, J.R., Komatsu, G., Baker, V.R., 1999. Geologic map of the Barrymore Quadrangle (V-59), Venus. U.S. Geological Survey Sci. Inv. Map I-2610
  34. ↑ Campbell, B.A., Campbell, P.G., 2002. Geologic map of the Bell Regio Quadrangle (V-9), Venus. U.S. Geological Survey Sci. Inv. Map I-2743.
  35. ↑ Hansen, V.L., DeShon, H.R., 2002. Geologic map of the Diana Chasma Quadrangle (V-37), Venus. U.S. Geological Survey Sci. Inv. Map I-2752
  36. ↑ McGill, G.E., 2004. Geologic map of the Bereghinya Planitia Quadrangle (V-8), Venus. U.S. Geological Survey Sci. Inv. Map I-2794.
  37. ↑ Campbell, B.A., Clark, D.A., 2006. Geologic map of the Mead Quadrangle (V-21), Venus. U.S. Geological Survey Sci. Inv. Map 2897.
  38. ↑ Pettengill, G.H., Eliason, E., Ford, P.G., Loriot, G.B., Masursky, H., McGill, G.E., 1980. Pioneer Venus radar results: altimetry and surface properties. J. Geophys. Res. 85, 8261–8270
  39. ↑ Masursky, H., Eliason, E., Ford, P.G., McGill, G.E., Pettengill, G.H., Schaber, G.G., Schubert, G., 1980. Pioneer-Venus radar results: geology from the images and altimetry. J. Geophys. Res. 85, 8232–8260.
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  41. ↑ Pronin, A.A., 1992. The Lakshmi phenomenon. In: Barsukov, V.L., Basilevsky, A.T., Volkov, V.P., Zharkov, V.N. (Eds.), Venus Geology, Geochemistry, and Geophysics (Research Results from the USSR). University Arizona Press, Tucson, London, pp. 68–81.
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  43. ↑ Head, J.W., Crumpler, L.S., Aubele, J.C., Guest, J.E., Saunders, R.S., 1992. Venus volcanism: classification of volcanic features and structures, associations, and global distribution from Magellan data. J. Geophys. Res. 97, 13153–13197.
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  51. ↑ 51.0 51.1 Ivanov, Mikhail A., and James W. Head. Geologic Map of the Nemesis Tesserae Quadrangle, V-13, Venus. US Department of the Interior, US Geological Survey, 2005.
  52. ↑ Hansen, Vicki L. "Venus's shield terrain." Geological Society of America Bulletin 117.5-6 (2005): 808-822.
  53. ↑ Ivanov, M. A., and J. W. Head. "Volcanically embayed craters on Venus: testing the catastrophic and equilibrium resurfacing models." Planetary and Space Science 106 (2015): 116-121.
  54. ↑ Tanaka, Kenneth L., et al. The Venus geologic mappers' handbook. No. 93-516. US Geological Survey, 1993.
  55. ↑ Rosenberg, Elizabeth, and George E. McGill. Geologic map of the Pandrosos Dorsa quadrangle (V-5), Venus. US Department of the Interior, US Geological Survey, 2001.
  56. ↑ Geological Survey (US), Leslie F. Bleamaster, III, and Vicki L. Hansen. Geologic map of the Ovda Regio Quadrangle (V-35), Venus. US Department of the Interior, US Geological Survey, 2005.
  57. ↑ Bannister, Roger A., and Vicki L. Hansen. Geologic map of the Artemis Chasma Quadrangle (V-48), Venus. US Department, of the Interior, US Geological Survey, 2010.
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