Design of a direct‑detection wind and aerosol lidar for mars orbit

The present knowledge of the Mars atmosphere is greatly limited by a lack of global measurements of winds and aerosols. Hence, measurements of height-resolved wind and aerosol profiles are a priority for new Mars orbiting missions. We have designed a direct-detection lidar (MARLI) to provide global measurements of dust, winds and water ice profiles from Mars orbit. From a 400-km polar orbit, the instrument is designed to provide wind and backscatter measurements with a vertical resolution of 2 km and with resolution of 2° in latitude along track. The instrument uses a single-frequency, seeded Nd:YAG laser that emits 4 mJ pulses at 1064 nm at a 250 Hz pulse rate. The receiver utilizes a 50-cm diameter telescope and a double-edge Fabry-Pérot etalon as a frequency discriminator to measure the Doppler shift of the aerosol-backscatter profiles. The receiver also includes a polarization-sensitive channel to detect the cross-polarized backscatter profiles from water ice. The receiver uses a sensitive 4 × 4 pixel HgCdTe avalanche photodiode array as a detector for all signals. Here we describe the measurement concept, instrument design, and calculate its performance for several cases of Mars atmospheric conditions. The calculations show that under a range of atmospheric conditions MARLI is capable of measuring wind speed profiles with random error of 2–4 m/s within the first three scale heights, enabling vertically resolved mapping of transport processes in this important region of the atmosphere.


Introduction
Previous space-based measurements [1][2][3][4][5] and modeling [6,7] have been used to study Mars atmospheric processes. Observations show that the main variability in the present Mars climate is related to variations in the spatial and temporal distribution of dust and water ice aerosols [8,9]. Dust interacts strongly with infrared radiation, which leads to changes in the thermal structure and acts as a driver of atmospheric motions at all spatial scales [10]. Water ice clouds play an important role in the water cycle altering the global transport of water vapor, including to active surface briny water flows (i.e., recurring slope lineae) [11,12]. The vertical distributions of dust and water ice aerosols exhibit complex structures that are not well-understood [13,14]. Observations using imaging and spectroscopic instruments on Mars orbiters [13,[15][16][17][18][19] have shown a wide variety of unexpected behavior including detached clouds, inversions in aerosol vertical profiles and very high altitude clouds. New measurements of the diurnal variations of aerosols, water vapor abundance, and winds [20,21] are still required to answer some important questions.
Despite low atmospheric density, the winds are often strong enough to raise large amounts of dust from the surface, and at times the planet can become almost completely enshrouded in it (see [16,22] for one such example). The winds transport water vapor, dust and ice aerosols, and mix all atmospheric gaseous constituents. Wind erodes the surface to create dust and sand particles and then transports these aeolian deposits, reshaping the surface geology. Winds regulate the transfer of water vapor and heat throughout the atmosphere and are a primary player in all surface-atmosphere interactions. Wind velocities provide sensitive input and validation for Global Circulation Models (GCMs), and are important for the safety and precision of spacecraft entry, descent and landing (EDL). Finally, Mars weather and wind predictions are important since dust storms and high winds affect mission operations on the surface that require visibility and consistent solar irradiation [16,23,24].
Despite their importance, there are very few direct observations of Mars winds. Current knowledge relies on a few cloud and wind streak observations, isolated observations from the Viking and Mars Science Laboratory landers [25,26], and indirect inferences of wind speeds that are often imprecise and contain many assumptions (e.g., [27]). The ability to sample wind profiles globally at all times of day and throughout seasons will also directly address science goals relating to the water cycle [11,12,28]. In addition to present day atmospheric processes, comparison of current wind values with recent and varying aeolian features will yield information on formation mechanisms, rates of change, and historical wind trends [30][31][32]. The 2011 Planetary Science Decadal Survey and the Mars Exploration Program Analysis Group (MEPAG) Goals Documents have cited several investigation aims that would be directly addressed by aerosol and wind measurements from orbit [21,33], and knowledge of winds remains a key "knowledge gap" for future human exploration of Mars.

Lidar overview
We have designed a direct-detection Doppler wind lidar for Mars orbit (MARLI) to address these needs. It is designed to provide vertically-resolved profiles of dust, water ice, and line-of-sight (LOS) winds to the surface, globally in all seasons day and night [34][35][36][37][38]. MARLI is designed to operate from a spacecraft in a circular polar orbit at a nominal altitude of 400 km. MARLI will be pointed 30° off-nadir in the cross-track direction, allowing for retrieval of cross-track wind profiles as shown in Fig. 1.
A block diagram of the instrument design is shown in Fig. 2. The lidar transmitter is a frequency-locked, diodepumped Nd: YAG laser that emits optically polarized pulses at 1064 nm. The MARLI receiver measures the verticallyresolved aerosol scattering profiles in the same polarization, as well the backscatter profiles that are cross-polarized. The parallel polarized backscatter profiles are passed through a solid, fused-silica Fabry-Pérot etalon used as a frequency discriminator, and their Doppler shifts are measured via the double-edge Fabry-Pérot lidar technique [39][40][41].
The present layout of the MARLI lidar is shown in Fig. 3. The current estimates of instrument payload parameters are a mass of 36 kg, operating power of 81 W, and data rate of 50 kbit/s. These parameters are nominal and were derived from the prototype versions of the laser, telescope, receiver optics, and detector.
In the remaining sections we describe the MARLI Doppler and polarization measurement approaches. Next, we provide a description of the major elements of the prototype instrument and discuss our method of determining the laser frequency and Doppler accuracy. We then present Mars atmospheric conditions from measurements taken by the Mars Climate Sounder used to calculate the expected instrument performance. Finally, we present a lidar model and estimate the measurement performance. We also briefly discuss our ongoing work to mature the technical readiness of the MARLI instrument to prepare for its consideration for a space mission.

Measurement approach
In orbit the MARLI instrument is designed to be nominally pointed at 30° from nadir in the cross-track direction. Its laser emits stable narrow linewidth laser pulses at a 250 Hz rate. The lidar receiver measures range-resolved backscatter profiles of the Mars atmosphere in three channels. The MARLI transmitted laser pulses are highly polarized (100:1). Two of the receiver channels measure the parallelpolarized backscatter but their passbands in frequency are slightly offset from one another to resolve the Doppler shift caused by wind-blown aerosols. The third channel measures the cross-polarized laser backscatter and is not Doppler resolved. The cross-polarized profiles can be used to detect and profile scattering from ice crystals that form clouds on Mars [42,43].
The laser photons that are scattered by aerosols back toward the lidar undergo a frequency shift due to the Doppler This allows MARLI to use the stronger Nd:YAG laser emission at 1064 nm, in contrast with lidar approaches for measuring winds in Earth's atmosphere that use the second (532 nm) or third harmonic (354.7 nm) wavelengths [44,45].
Historically several types of spectral filters have been used in direct detection Doppler lidar receivers, including approaches based on etalons, absorption lines [46], Fizeau interferometers [47], fringe imaging [48], and Mach-Zehnder interferometers [49,50]. The MARLI optical receiver uses a frequency discriminator based on the double-edge Fabry-Pérot etalon (DEFP) technique [40,[51][52][53]. Using a single edge technique, high measurement sensitivity of the LOS aerosol motion was achieved using the edge of a spectral filter [41]. The use of a second filter edge (i.e. double-edge) increases the measurement sensitivity resulting in a 1.6-times improvement in the measurement accuracy [40]. The double-edge technique involves locking the laser frequency at the crossing point (i.e. the half-widths) of two filter edges of opposite slope and measuring the changes in signal through the two filters simultaneously. We chose the DEFP technique with a solid etalon for MARLI due to its simplicity, ruggedness, and its compatibility with the number of pixels available in the lidar detector.
In the MARLI receiver design a single etalon is used for both edge filters, similar to the design described by Kim et al. [54]. Briefly, the laser backscatter that is collected by the receiver telescope is split into two paths, which are directed through a solid, fused silica Fabry-Pérot etalon at two slightly different angles. One of the paths is normally incident on the etalon front surface while the other is offset by 1.2 mrad. After passing through the etalon both paths illuminate separate detector elements. This angular offset shifts the optical passband frequency for the offset path, and both paths together form a simple double-edge frequency discriminator. When the laser frequency is locked to the crossing point of the two filters the zero-Doppler-shift point is at the maximum slopes of the two passbands. With an etalon, the angular offset of the second path causes a slightly lower transmittance and slightly broader, asymmetrical bandwidth for that path, which does slightly degrade the measurement precision [55]. The prototype laser transmitter was designed and constructed by Fibertek, Inc. and leveraged some elements of an earlier laser design used in the Cloud-Aerosol Transport System lidar [56]. The Nd:YAG laser is a Q-switched master-oscillator power-amplifier (MOPA) design using a tunable single frequency seed laser, a ring oscillator, and a single stage power amplifier.
The MARLI laser requires a low power single frequency laser to seed the laser's ring oscillator in order to maintain a stable single frequency emission. Our approach uses a micro-non-planar ring oscillator (µNPRO) that is being developing for the Laser Interferometer Space Antenna (LISA) mission [57]. The µNPRO allows higher power and narrower, and much more stable linewidth than a diode seed laser in a small, efficient package. The present µNPRO layout is shown in Fig. 4. Figure 5 shows the layout of the laser transmitter with optics and the amplifier on the front face, and the electronics and laser output on the opposite face, along with the single cold plate for connection to an external heat pipe or liquid cooling plate. The laser parameters are listed in Table 1 along with specifications for the telescope, receiver optics, and detector.
The lidar receiver uses a Cassegrain telescope made of beryllium that has a 50-cm diameter and a 2-m effective focal length. The telescope optical surfaces are gold coated with a sunshield surrounding the primary mirror that may also be used as a thermal radiator. From the field stop, the received light is recollimated to a beam diameter of 50 mm to fill the etalon's clear aperture. The received photons then pass through the spectral filter assembly, which includes (in series) a bandpass filter, a gapped etalon, a diffractive optical element (DOE), and the fused-silica (fine) etalon that forms the double-edge filter. Plots of the frequency-dependent transmission of each element in the serial filter stack are shown in Fig. 6.
The bandpass filter (black curve in Fig. 6a-c) blocks most of the solar background. Its transmission peak was designed to be sufficiently narrow to block all but one passband of the coarse etalon (green curve). Although five resonance peaks of the fine etalon are contained within the FWHM of the coarse etalon bandwidth (Fig. 6b), this configuration allows sufficient optical transmission at the laser wavelength while also minimizing the daytime optical background to the detector. The cumulative transmission losses of the three elements combined with locking the frequency to the edge of the fine etalon at the half-width point results in an overall filter stack transmission of 32% for each of the double-edge Doppler channels.
After the coarse etalon the optical signal passes through a polarizing beamsplitter (PBS). It reflects parallel-polarized light towards the DOE and the double-edge filter, while the perpendicularly-polarized light is transmitted through the PBS towards a second optical path that bypasses these elements. The linear depolarization ratio of the backscattered profile can be calculated from the measurements of the signal through each of the edge filter channels  Two views of the MARLI laser optical bench. a A layout drawing of the laser's optical bench. The red line traces the laser beam path from the seed on the left-hand side through to the periscope on the right lower section, after which the beam is expanded before exiting the laser on the back face. b A photograph of the same side of the as-built laser prototype during assembly from the same viewpoint. The approximate dimensions are 40 cm by 22 cm by 15 cm. The seed laser stage is not shown (parallel-polarization) and that from the perpendicular polarization channel, yielding information on the vertical distribution of ice crystals [43].
The two beams from the fine etalon and the one from the cross-polarized channel are focused in three 113 µm diameter spots on the HgCdTe APD surface. Each of the beams is focused onto separate 2 × 2 pixel quadrants of the detector. The HgCdTe APD has an APD gain of up to 900 and a 0.4 fW/Hz 1/2 noise equivalent power [58][59][60][61]. The detector chip and preamplifer are mounted within an integrated detector cooler assembly (IDCA) are shown in Fig. 7. A similar version of this IDCA was developed to TRL-6 under the NASA In-Space Validation of Earth Science Technologies (InVEST) program [62].
The MARLI receiver electronics sum the signals from the four pixels in each quadrant of the detector and digitize the signals from the three channels with an analog to digital converter (ADC). The ADC subsystem will measure the detector signal levels in 500 ns bins (corresponding to a 75-m vertical bins) for every laser pulse. Every 0.5 s the lidar will record the range-resolved measurements of the atmospheric backscatter in both parallel channels, and ratios of cross-to parallel-polarized backscatter will be recorded, along with instrument housekeeping data. After averaging those records, the LOS and horizontal wind profiles, the parallel polarized aerosol profile and the profile of the cross-polarized backscatter scatter will be computed. Although the amount of both the vertical and horizontal averaging are flexible, our performance analyses are based on using averaging of 2 km vertically and 2 degrees of latitude (40 s) horizontally.

Doppler accuracy and bias control
Accurate retrieval of the wind-induced Doppler shift depends on knowledge of the relative frequency offset of the transmitted laser pulses and the crossing-point of the double edge filter. Several factors can contribute to this offset including laser frequency stability, temperature changes of the double-edge filter, and the velocity of the surface with respect to the orbiting instrument. We discuss our monitoring and compensation approaches for these potential sources of bias below.
A seed laser is used to stabilize the center frequency of the ring oscillator of the laser transmitter. When first starting the laser, its frequency may be several gigahertz away from the double-edge filter's zero-crossing point. For broad frequency tuning, the seed laser's frequency can be tuned via temperature tuning of the seed laser crystal. To stabilize the laser frequency and/or offset a known bias, the seed laser frequency can be tuned at the MHz level via piezoelectric tuning the seed laser crystal.
We have developed a two-stage wavelength monitor subsystem that continuously samples the outgoing laser wavelength to monitor the seed laser's frequency as shown in Fig. 8. Our approach first directs a small portion (< 1%) In the present design, a second, finer wavelength monitor stage utilizes the small area of the fine etalon in the receiver subsystem that is shadowed by the telescope secondary. We first direct a small portion of the transmitted laser energy via a single-mode optical fiber to the receiver subsystem. This monitor signal is directed from the optical fiber to a small mirror suspended via support vanes in front of the center of the diffractive optical element. This creates two monitor beams that are offset in angle by 1.2 mrad. After the monitor beams pass through the etalon, a second small mirror reflects the two monitor beams out of the main receiver path and a focusing lens images them onto two elements of a silicon detector. The ratio of the signals on the two elements is used to tune and lock the seed laser frequency to the crossing point of the double edge filter. A similar wavelength tracking method was used successfully in the 532 nm receiver channel of the GLAS lidar on the ICESat mission [64].
The passbands of the double-edge filter are also temperature sensitive, so changes in its temperature can also introduce Doppler bias into the measurements. The temperature-dependence of the index of refraction of fused silica causes the passband frequency to shift by 355 MHz for every 1 °C temperature change. For MARLI this leads to a requirement that the temperature of the fused silica etalon be held to ± 5 mK for a passband stability of 1.77 MHz. In addition, the thermal gradients within the etalon must be minimized. Our present approach is to enclose the receiver's optical subsystem in a warm-biased insulated thermal enclosure (as in [45]), and to stabilize the enclosure's temperature.
In addition to instrument effects the rotation of Mars will induce a latitude-dependent sinusoidal Doppler signal caused by the cross-track pointing and polar orbit. Its amplitude is ~ 213 MHz and its period is ~ 2 h. The slow predictable nature and amplitude of this effect allows it to be compensated via piezoelectric tuning of the seed laser's frequency. The lidar return from the Mars surface may also be used as a reference for the transmitted laser frequency. The ratio of the surface return from the two Doppler channels can be used to monitor the relative offset of the laser frequency from the crossing point of the double-edge filter. This technique has the benefit of using the same optical path as the atmospheric backscatter signal.

Instrument performance model
We have developed a statistical model of the MARLI lidar measurements to guide instrument design and to predict the lidar's performance in orbit. Our approach builds on previous space lidar measurement models which we have developed while building and operating the Mars Orbiter Laser Altimeter (MOLA), the Geoscience Laser Altimeter System (GLAS) atmospheric lidar channel, the Mercury Laser Altimeter (MLA), and the Lunar Orbiter Laser Altimeter (LOLA). The model uses the demonstrated laser pulse energy and width, optical receiver parameters, and the detector response and noise characteristics. The instrument parameters are listed in Table 1, and detector characteristics can be found in recent publications [59,65].

Models of the mars atmosphere
In order to estimate MARLI performance we selected several cases that represent the atmosphere under a range of atmospheric aerosol (dust and water ice) loading. Observations of the Mars atmosphere have revealed complex interactions between its dust, water and CO 2 cycles [5,8,66]. The bulk of current spacecraft observations of the global Mars atmospheric state come from the Mars Global Surveyor (MGS) and Mars Reconnaissance Orbiter (MRO) spacecraft, which show large temporal variations in the amount and vertical distribution of dust and ice aerosols and water vapor [13,17]. For this work we extracted aerosol profiles using extinction profiles (version 5.2.4) from the Mars Climate Sounder (MCS) on the MRO [67][68][69]. The MCS extinction retrievals were then scaled to the MARLI wavelength of 1064 nm [70]. We chose to neglect molecular scattering since it is so small at the low atmospheric pressure of Mars [9].
The first atmospheric case was chosen to represent a relatively dust-free atmosphere, where water ice scattering would make up a significant portion of the backscattered signal. This was drawn from MCS data averaged over Northern Hemisphere spring (L s = 5°-30°) of Mars year 34 (MY34) northern latitudes (60° N-80° N). The second case was an average from Southern Hemisphere spring (L s = 150°-230°) of MY33 mid-latitudes (50° S-25° N), representing an  For these models the extinction to backscatter ratio for dust was assumed to be 40 steradians based on measurements made by the lidar on the Mars Phoenix lander mission [71]. This ratio is also consistent with values for desert aerosols on Earth [72]. For water ice the extinction to backscatter ratio was assumed to be 15 steradians based on measurements from the Mars Phoenix lidar [73]. The cirruslike nature of clouds on Mars [42] led us to assume an ice depolarization ratio ( ⊥ ∕ ∥ ) of 0.47, taken from 1064 nm elastic lidar measurements of cirrus clouds [74] that formed above Earth. The parallel-polarized backscatter signal is thus a combination of scattering from dust and ice, while the perpendicularly-polarized backscatter was assumed to be from ice. The backscatter profiles used to determine the instrument performance are the attenuated parallel (Fig. 9a) and perpendicular (Fig. 9b) profiles for each of the three atmospheric cases.

Double-edge Fabry-Perot Etalon
The optical transmission wavelength [75] of the receiver's fine etalon is given by where pk is the peak transmission, F is the finesse of the etalon, F is the free spectral range, , , F is the phase delay of the light after each pass through the etalon, is the optical wavelength, and is the light incident angle. The phase difference in Eq. (1) is given by with c the wavelength at the peak transmission and n E is the etalon index of refraction. For a fused silica etalon n E = 1.45 . The center wavelength is rounded to the nearest integer value for mathematical convenience. In practice, the etalon wavelength is temperature-tuned to within the operating range of the laser.
The fine etalon design for MARLI has a peak transmission of 70%, a free spectral range of 2.5 GHz and a pass band of 0.1 GHz. The rest of the etalon parameters can be derived [75] and are listed in Table 1. For illumination at small offsets from normal incidence, the etalon transmission is similar to that at normal incidence, but the peak transmission is shifted slightly longer in wavelength and the peak becomes asymmetrical, broadening on the higher frequency edge [55,76]. We note that an accurate calculation of the full etalon response for this beam would include effects of a three-dimensional beam with finite divergence [77]. Our simplifying approximation of using two symmetrical filter edges was made because in the DEFP method the received signal only passes through the low-frequency edge of the off-axis bandpass. In practice we can also measure the etalon transmission versus frequency for both beams once the etalon is mounted in the receiver subsystem to determine the actual double-edge response function.
For the double-edge wind measurement, the MARLI approach calculates the ratio of the difference to the sum (RDOS) of the signals through the etalon as Fig. 9 The Mars atmospheric backscatter profiles used to predict MARLI measurement performance were computed from MCS retrievals. a Attenuated backscatter (βT 2 ) with polarization parallel to the transmitter for the three atmospheric test cases as a function of altitude. b Attenuated backscatter with polarization perpendicular to the transmitter for the same three cases where f DE ( ) is the double-edge etalon response function, and E0 ( ) and E1 ( ) are the etalon transmission at the normal and slightly off-axis incidence angles, and λ is the Doppler-shifted wavelength. The off-axis angle is chosen such that the low-frequency edge of the off-axis etalon transmission curve crosses the on-axis etalon transmission curve at the midpoint, as shown in Fig. 6. The Doppler shift in the backscattered signal is related to the wind speed v w by where c the speed of light and λ 0 is the transmitted laser wavelength. The Doppler profile in the LOS direction can be expressed as is the inverse function of Eq. (3), which can be obtained numerically, and N s0 (h) and N s1 (h) are the net received signal through the etalon in the on-axis and offaxis channels integrated over a given atmosphere layer and a number of repeated measurements. Figure 10 shows a plot of the RDOS of the etalon transmission as a function of the cross-track horizontal wind speed. The derivative of the RODS with respect to the wind speed is also plotted. We designate this derivative as the Error Multiplier, which is the factor by which the sensitivity of the double edge filter is reduced as the Doppler shift increases in amplitude. The plot shows the present MARLI etalon design allows estimating horizontal wind speeds to ± 60 m/s in the viewing direction and that wind speeds of ± 45 m/s can be measured with an Error Multiplier < 3.

Expected wind measurement uncertainty
The lidar receiver signal passing through the double-edge filter in the on-axis direction can be written as [78], where N s0 (h) is the total number of the integrated signal photons from the on-axis path from the atmosphere layer at altitude h of thickness ΔH (2 km) and from averaging time, T av , of 40 s, hf is the photon energy, E t is the laser pulse energy, (h) is the atmosphere volume backscatter coefficient per polarization axis in 1/m-sr at altitude h , T 2 (h) is the two-way optical transmission of the atmosphere layer being measured, 2 a is the two-way transmission from the upper atmosphere not included in T 2 (h) , O is the optical transmission of the MARLI receiver optics including the bandpass filter, polarization beamsplitters, and coarse etalon, A T is the receiver telescope aperture area, H s is the spacecraft orbit altitude, p is the laser beam pointing angle from nadir direction, and E Δ D is the on-axis etalon transmission with Doppler shift Δ D due to the LOS wind. The signal passing through the etalon at the off-axis angle can be calculated by replacing E0 Δ D with E1 Δ D in Eq. (6).
The average background photons per range bin detected by the receiver can be calculated from where I is the spectral irradiance from the Sun (277 W/m µm) at 1064 nm, is the assumed surface reflectance (0.26), Δ f is the equivalent filter bandwidth calculated from integrating the filter stack transmission over the passband, and FOV is the receiver field of view. The factor of ½ in Eq. (7) accounts for the effect of the polarization beamsplitter which reflects ½ the solar background light. There is also detector dark noise N D which is 55 kHz for each pixel, with four pixels being summed per channel for a dark noise rate of 220 kHz. The integration time for the SNR computations is 40 s (10,000 shots) and measurements are made in 2-km range bins (ΔH).
For the HgCdTe APD detector used in MARLI, the performance is nearly shot-noise limited [59] and hence the variance of the detected signal can be approximated by the The noise terms from the background photons and dark counts are multiplied by two because the approach separately estimates the background between the laser pulses and subtracts it from the total when the laser pulse is present. The random error in the wind velocity measurement can be approximated by multiplying results from Eq. (8) by the error multiplier given in Fig. 10.
To determine a nominal wind speed with which to calculate instrument performance, we calculated the mass (i.e. pressure) weighted wind speed on Mars (combining the zonal and meridional winds) over the entire year over the globe. The result was an average speed of 18 m/s. The results of the instrument model are shown in Fig. 11 for a crosstrack, horizontal nominal wind speed of 18 m/s. The results of the instrument model suggest the instrument is particularly sensitive to wind in the lower atmosphere, with random error between 1.5 and 6 m/s (for dust storms) at the surface.
The scale height of the Mars atmosphere is ~ 11.1 km, and approximately 95% of the atmospheric mass is contained in the lowest 3 scale heights. The MARLI performance models show its wind speed retrievals typically show random errors < 4 m/s in the lowest ~ 3 scale heights under the three dust-loading conditions considered. Since the vast majority of atmospheric transport of dust, water, and trace species occurs in this region of the atmosphere MARLI's precision enables discrimination of the transport characteristics of the mean atmospheric circulation (i.e., the Hadley circulation) and intermittent/irregular processes such as baroclinic and barotropic waves, atmospheric tides, and stationary waves. Understanding Mars atmospheric transport is key for resolving long standing questions about the Mars atmosphere and climate. This precision is also sufficient for evaluating general circulation models and for assimilating MARLI measurements into improved atmospheric models.

Relative error of atmospheric backscatter profile measurements
The characteristics of the backscatter profile measurement were calculated in a similar manner, but by summing the signals from the normal incidence and off-axis signals from Eq. (6). Figure 12a shows the relative error, defined as the ratio of the standard deviation to the mean for the atmosphere backscatter profile measurements in the parallel polarization. The relative error for the cross-polarization (perpendicular) channel was obtained similarly by using the passband width for the coarse filter only and the optical transmission without the etalon and the beam splitting optics. The uncertainty in depolarization ratio can be calculated from the relative errors of the parallel and perpendicular polarization channels. MARLI's sensitivity to dust and water ice aerosols is particularly advantageous in the atmospheric boundary layer and lowest pressure scale height in the atmosphere, where existing observations (e.g., from MCS and the Thermal Emission Spectrometer) are either insensitive (due to high line-of-sight opacity in limb-viewing geometry) or have only coarse resolution. This unique ability to resolve the near-surface region of atmosphere at 2 km vertical resolution will help resolve questions regarding dust lifting processes, sources and sinks of dust, and how dust is transported through the atmosphere. Additionally, MARLI's 2 km vertical resolution is superior to existing dust observation climatologies and will help better resolve mesoscale phenomena such as high-altitude dust layers and dust plumes. Fig. 11 The RMS wind-speed uncertainty from the MARLI instrument model computed as a function of altitude from the surface for the case of a uniform cross-track horizontal wind speed of 18 m/s. This uncertainty will be modified at different wind speeds via the error multiplier shown in Fig. 8

Future work
We are currently building a prototype instrument using a prototype laser transmitter and the optical receiver described above with a 14-cm diameter receiver telescope, and the integrated detector-cooler assembly. Our plans are to demonstrate wind measurements using lidar backscatter from thin cirrus clouds in Earth's atmosphere, which approximate the backscatter characteristics of the Mars atmosphere. We are also testing the thermal design of the double-edge filter assembly to verify its performance in air and in vacuum. In addition, we will continue to develop our instrument model to include factors such as laser frequency stability and etalon thermal stability. We will also perform a trade study to optimize the passband width of the double-edge filter based on the expected dynamic range of winds in the Mars atmosphere. The objective is to find the best tradeoff between using a broader linewidth etalon to expand the wind measurement dynamic range versus the impact of increasing the wind measurement uncertainty at lower wind speeds.

Summary
We are developing MARLI, a direct detection wind and aerosol lidar for Mars orbit. The design uses a pulsed singlefrequency Nd:YAG laser and the double-edge Fabry-Pérot technique to resolve the Doppler shift in the atmospheric backscatter profiles. MARLI is being designed to provide global, height-resolved measurements of LOS winds, aerosol backscatter, and depolarization ratio. We have developed an instrument performance model that includes measured atmospheric scattering for a range of Mars atmospheric conditions. The performance has been calculated assuming averaging of 40 s (2° in latitude) with a vertical resolution of 2 km. The results show typically < 4 m/s random error wind measurements from the surface to 35 km. We have developed breadboards and prototypes of the laser, wavelength locking method, the receiver optics, and detector. Ongoing work involves completing the prototypes and demonstrating measurements to thin cirrus clouds in Earth's atmosphere.
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